Skip to main content

Thank you for visiting You are using a browser version with limited support for CSS. To obtain the best experience, we recommend you use a more up to date browser (or turn off compatibility mode in Internet Explorer). In the meantime, to ensure continued support, we are displaying the site without styles and JavaScript.

Vegetation response to exceptional global warmth during Oceanic Anoxic Event 2


The Cenomanian–Turonian Oceanic Anoxic Event (OAE2; ~94.5 million years ago) represents an episode of global-scale marine anoxia and biotic turnover, which corresponds to one of the warmest time intervals in the Phanerozoic. Despite its global significance, information on continental ecosystem response to this greenhouse episode is lacking. Here we present a terrestrial palynological record combined with marine-derived temperature data (TEX86) across an expanded OAE2 section from the Southern Provençal Basin, France. Despite high TEX86-derived temperature estimates reaching up to 38 °C, the continental hinterland did support a diverse vegetation, adapted to persist under elevated temperatures. A transient phase of climatic instability and cooling during OAE2 known as Plenus Cold Event (PCE) is marked by the proliferation of open, savanna-type vegetation rich in angiosperms at the expanse of conifer-dominated forest ecosystems. A rise in early representatives of Normapolles-type pollen during the PCE marks the initial radiation of this important angiosperm group.


Past time intervals of exceptional climatic warmth, typically associated with elevated pCO2, had profound impacts on floral compositions and biogeographic patterns of continental vegetation1,2,3. Within the overall greenhouse climate characterizing the Mesozoic, the Late Cretaceous Oceanic Anoxic Event (OAE) 2, which spans the Cenomanian–Turonian boundary [94.1 million years ago (Ma)], marks the onset of an extreme phase in ocean temperatures known as the “Cretaceous thermal maximum”4,5,6. This phase is characterized by one of the highest (>35 °C) proxy data-derived sea-surface temperature (SST) estimates of the last 150 Myrs, which are recorded by both planktonic foraminifera δ18O and archaeal membrane lipid-based TEX86 data6. A significant rise in low- and mid-latitude open ocean SSTs (2–4 °C) and mid-latitude shelf-sea temperatures (4–5 °C) accompanied the onset of OAE2, resulting in the Late Cenomanian–Turonian hothouse5,7,8,9. Besides the exceptional thermal conditions, the OAE2 (lasting 700–800 kyrs10,11) is associated with widespread formation of organic-rich deep-water deposits12,13, a major positive carbon isotope excursion (CIE) in carbonate and organic carbon reflecting massive burial of 13C-depleted carbon14,15, and major biotic turnover in marine ecosystems16,17.

Despite the outstanding position of OAE2 as one of the most remarkable events of the Mesozoic18, the responses of terrestrial ecosystems and continental flora to the changes of the global climate system remain largely unexplored. To date, just a few isolated plant macrofossil discoveries have been reported from the organic-rich Bonarelli Level, which is the sedimentary expression of the OAE2 in Marche–Umbria, Italy19. Microfloral evidence is essentially lacking due to the overwhelming predominance of amorphous kerogen in most marine OAE2 black shales, diluting any continent-derived spore-pollen signal. However, based on a shift in the δ13C signature of leaf-wax n-alkanes, a change from C3 to C4-dominated low-latitude vegetation triggered by a pCO2 drop has been proposed20 for the early phase of OAE2. According to theoretical considerations21, the exceptional warmth that prevailed during Late Cenomanian–Turonian times may have exceeded the heat tolerance of continental ecosystems, which potentially resulted in widespread vegetation dieback.

Here we present a high resolution and taxonomically differentiated spore-pollen record across a stratigraphic interval correlating to the OAE2. The record is from an expanded marine section (Cassis) from the Southern Provençal Basin (SPB) of S’ France (Fig. 1) and has been analyzed for biostratigraphy, palynology, TEX86 and stable carbon isotopic composition of carbonates and organic materials. Stratigraphic assignment of the section is based on existing ammonite data22 combined with new information from planktonic foraminifera, calcareous nannoplankton, and carbon isotopes of bulk carbonate, organic matter and plant wax-derived long-chain n-alkanes.

Fig. 1

Palaeogeographic map illustrating Cenomanian–Turonian biome distribution. Palaeo-map is modified after ref. 48 and includes the extent of the Normapolles palynofloral province29. Color code representing (A) tropical moist, open canopy mixed forest with shrub understory; (B) savanna-type dry low understory with sparse trees; (C) deciduous dry/warm shrubland; (D) mid-latitude evergreen closed canopy conifer forest; (E) Normapolles province; (F) evergreen wet/cool shrubland; (G) high-latitude moist, open canopy forest with shrub understory; (H) boreal closed canopy conifer forest. Asterisk marks approximate location of the Southern Provençal Basin



The ~235 m thick Cassis section represents a heterolithic succession with its lowermost part being composed of clays and marls overlain by (in part) turbiditic sandstones (0.0‒19.7 m). An exposure gap in the outcrop separates the siliclastic facies from a conspicuous limestone slope deposit characterized by intense slumping and disintegration (33.4‒46.1 m). Above another exposure gap, the main part of the section is continuously accessible (55.8‒236.0 m) and consists of homogenous marls with intercalated bundles of nodular limestone together representing basinal facies. Existing ammonite data combined with new biostratigraphic results constrain this section to the Upper Cenomanian–Lower Turonian22 (Supplementary Note 1). This age assignment is further corroborated and refined by carbon isotope data, which show a characteristic positive CIE revealing an initial high-amplitude positive peak (a) followed by a trough interval, which gives way to a plateau with two consecutive peaks (b, c) (Fig. 2). The characteristic pattern of the CIE is mimicked in the δ13Corg signature of bulk organic matter (Supplementary Fig. 1) and corroborated by the isotopic composition of long-chain n-alkanes derived from plant leaf-wax. Backed by high-resolution biostratigraphic data, the CIE evolution can be closely correlated with the reference carbon isotope record from Eastbourne, UK23,24 (Fig. 2). The significantly increased δ13Ccarb values of the CIE peak (a) at Cassis (6.0‰) compared to Eastbourne (4.8‰) may reflect a shift in the dominant carbonate source in the SPB during this particular interval. In fact, the Calcaires du Corton Fm. corresponds to a calcareous unit composed of upper slope deposits, which can be traced toward the shoalwater carbonate platform bordering the SPB to the north where similarly high δ13Ccarb signatures are observed in OAE2-equivalent platform limestones25. Carbonate carbon isotope signatures > 6.0‰ for the OAE2 CIE are also described from the epeiric Iberian seaway26 and may reflect variations in the aragonite content of the periplatform ooze exported from the adjacent platform27. The correlation thus reveals very good stratigraphic coverage of the uppermost Cenomanian–Turonian at Cassis with an expanded ~200 m thick OAE2 interval (Fig. 2). High sedimentation rates accompanied by increased input of continental organic debris in a transtensive geotectonic setting28 may have prevented the accumulation of black shales enriched in marine-derived organic carbon in the SPB.

Fig. 2

Bio- and chemostratigraphic correlation. Carbon isotope trend from Cassis, S’ France is compared with the European reference section at Eastbourne, Sussex, UK23,24. Calcareous nannofossil zonation of Eastbourne after ref. 56. Planktic foraminiferal biozonation of Eastbourne after ref. 69. Lowercase letters correspond to principal carbon-isotope peaks identified in the Eastbourne record24. Stratigraphic positions of the Plenus Cold Event (PCE) according to (1)53, (2)70, (3)13 with (4) representing supposed PCE position at Cassis. Color-code of the Cassis carbon-isotope record corresponds to lithostratigraphic formations22,28 with blue = Grès de l’Anse Sainte Magdeleine Fm., orange = Calcaires du Corton Fm., black = Marnes de l’Anse de l’Arène Fm. Carbon-isotope stratigraphic trend of plant-derived leaf-wax n-alkanes (n-C25; n-C27) is restricted to the Marnes de l’Anse de l’Arène Fm. δ13C values of individual n-alkanes are the means of duplicate runs (σ = ±0.5‰) expressed versus VPDB. Gray area represents the stratigraphic interval covered by the OAE2 carbon isotope excursion24,54. Note the expanded thickness of the OAE2 in the Cassis record


At Cassis, high numbers of inaperturate and bisaccate gymnosperm pollen (avg. = 48.2%) are essentially produced by Araucariaceae and Cupressaceae-type plants (Araucariacites spp.; Inaperturopollenites spp.) and Cheirolepidiaceae (Classopollis spp.) with subordinate contributions from Pinaceae (Cerebropollenites spp.) and Podocarpaceae (Podocarpidites spp.). Other gymnosperms, including cycads-ginkgophytes (Cycadopites spp.), gnetaleans (Ephedripites spp.), and seed ferns (Alisporites spp.) are quantitatively of minor importance (avg. = 2.5%). Spores produced by a diverse assemblage of ground ferns and fern allies occur in moderate quantities (avg. = 12.8%). The assemblage contains a variety of eudicotyledonous angiosperm pollen represented by various tricolporate and triporate types, the majority of which can be assigned to early forms of the Normapolles complex (predominantly Atlantopollis and Complexiopollis groups; avg. = 18.9%) (Supplementary Fig. 2).

Based on stratigraphic variations in relative spore-pollen abundances, six characteristic assemblage zones (AZ I–VI) are differentiated from base to top (Fig. 3). A pre-CIE assemblage (AZ I, 6.5–18.5 m) shows the lowest number of individual taxa (avg. = 30.2) and a moderately high gymnosperm to angiosperm (G/A) ratio (avg. = 0.65) with the angiosperm component being dominated by non-Normapolles-type pollen. Among conifer pollen, relatively high abundances of Cerebropollenites spp. (avg. = 7.3%) are paralleled by low Inaperturopollenites spp. content (avg. = 9.5%). The overlying assemblage (AZ II, 34.7–45.2 m) corresponds to the first build-up phase (peak a) of the CIE and shows increased total taxa counts (avg. = 39.9). An increase in Normapolles-type angiosperm pollen results in slightly lower G/A-ratios (avg. = 0.62). Conifer-derived Inaperturopollenites spp. remain similar (avg. = 10.6) but show a marked increase toward the top of AZ II reaching up to 22.9%. Above, the trough-shaped CIE interval corresponds to an assemblage (AZ III, 57.1–110.8 m) characterized by stable numbers of taxa (avg. = 40.1) and a low dominance index with average D values of 0.06 indicating a high degree of ecological evenness of the floral association. Increased abundances of Normapolles-type pollen (e.g., A. microreticulatus) are paralleled by low conifer pollen contents (e.g., Inaperturopollenites spp.) resulting in comparatively low G/A-ratios (avg. = 0.55). The onset of peak (b) is again characterized by an assemblage rich in conifer-derived grains and low angiosperm pollen (AZ IV, 114.2–143.2 m) with increased G/A-ratios (avg. = 0.70) and high dominance index (avg. = 0.09). Another increase in Normapolles-type pollen marks the overlying assemblage (AZ V, 146.3–149.4 m) which shows the lowest G/A-ratios (avg. = 0.41) paralleled by low D values of 0.06. Above, the upper part of the CIE plateau up to peak (c) corresponds to the topmost assemblage (AZ VI, 156.7–225.3 m). Here, the strong dominance of a few abundant conifer-derived pollen (with Inaperturopollenites spp. reaching up to 31.8%; avg. = 20.4%) causes substantially higher G/A-ratios (avg. = 0.77) and higher dominance indices (avg. = 0.12). Calculated origination and extinction records show very low values and the range-through diversity comparatively high and stable values throughout the studied interval, which are illustrating the absence of major land plant extinction during OAE2. Increased values at the base of the origination record and at the top of the extinction record, as well as reduced values at the base and the top of the range-through diversity trend are interpreted as consequences of edge effects.

Fig. 3

Terrestrial palynomorph and TEX86 data across OAE2. Stratigraphic trends in δ13Ccarb, δ13Corg, TEX86-derived sea-surface temperatures (SSTs) and evolution of palynofloral diversity and composition across OAE2 at Cassis, S’ France. Biostratigraphy and lithological log of Cassis section to the left. (A) Carbon-isotope stratigraphy based on bulk rock carbonate and organic matter; (B) TEX86 and SST reconstruction based on TEX86H calibration; (C) species richness; (D) dominance index; (E) stratigraphic distribution of selected pollen including the Normapolles-type angiosperm pollen Atlantopollis reticulatus and the conifer pollen Inaperturopollenites spp.; (F) ratio of gymnosperm versus angiosperm taxa; (G) assemblage zones (AZs) based on characteristic spore-pollen associations. PCE = Plenus Cold Event. Blue horizontal bands represent individual SST cooling episodes during the PCE

The overall rich and diverse palynological association obtained from Cassis is taxonomically distinctive for a position within the Late Cretaceous Normapolles phytogeographic province29. Stratigraphic trends in the distribution of the abovementioned groups and indices are considered to primarily reflect changes in the vegetation structure of the adjacent continental hinterland of the SPB.

TEX86 temperature estimates

SST estimates based on TEX86 show continuously high temperatures >35 °C for the SPB during Late Cenomanian–Turonian times with maximum SSTs reaching 38 °C (Fig. 3). These warm SSTs conform with existing TEX86 studies from early Late Cretaceous mid- and low-latitude sites5,6,8,9 and highlight the exceptional temperature regime prevailing during deposition of OAE2. A gradual SST decline is indicated by decreasing TEX86 values characterizing the latest Cenomanian to earliest Turonian at Cassis. In the SPB, the overall pattern of exceptional high temperatures is punctuated by several transient drops towards significantly lower TEX86 values (<0.8), which translate into SSTs below 32 °C. These cooler SST estimates characterize a phase of climatic instability and occur within an interval stratigraphically placed within the upper UC3 and UC4 nannofossil zone, below and close to the R. cushmani-W. archaeocretacea zone boundary and corresponds to the trough-shaped segment of the CIE between peaks (a) and (b).


Critically high temperatures have been put forward as a mechanism for the suppression of terrestrial plant and animal life during the end-Permian extinction and basal Triassic events30,31,32. For these intervals, exceptional climatic warmth is considered a first order control for the well-documented turnover in continental vegetation3,33. During the Cretaceous thermal maximum, exceptional warmth and associated heat stress have also been suggested to significantly affect plant growth by inhibiting photosynthesis to a certain extent at daytime temperatures ranging between 35° and 42 °C21. Continental temperatures in this range are considered life-limiting to plants, resulting in serious thermal stress and potential die-off34,35. However, the rich and diverse flora reconstructed from palynological datasets across the OAE2 does not support the idea of widespread heat-induced die-off in continental vegetation—at least not in the hinterland of the studied SPB. Despite maximum TEX86-derived SSTs of up to 38 °C reconstructed for the SPB, the hinterland supported a rich and diverse flora, which is roughly similar in composition to the type of vegetation thriving in Late Cenomanian to Early Turonian times in other parts of the palaeo-European archipelago36,37. Mid-latitude terrestrial plant ecosystems were apparently well adapted to the exceptional warm conditions prevailing during the Cretaceous thermal maximum. The potential effects of temperature extremes might have been more aggravated in continental interior regions of the subtropics and close to the equator, where even higher mean annual surface temperatures are to be expected38.

Despite the absence of major plant extinction associated with OAE2, variations in the relative contribution of individual taxa and groups reflect compositional changes in vegetation. High contents of Araucariaceae and Cupressaceae-derived pollen indicate the presence of forest communities composed of large trees forming a dense emergent cover39,40. An arborescent habit of Cretaceous araucarioids is supported by abundant fossil wood finds from mid-latitudes41 and in line with the growth habit of modern Araucaria types42. Together with high pollen abundances produced by Pinaceae, Podocarpaceae and xerophytic Cheirolepidiceae, this type of assemblage (AZ II, IV, and VI) is interpreted to reflect mixed forest dominated by arborescent conifers with an only moderate angiosperm component, which grew in mesic habitats with moderate availability of moisture. Such conifer-dominated ecosystems prevailed during episodes of increased δ13C values including the first build-up (peak a, AZ II), the second build-up (peak b, AZ IV) and upper plateau phase (AZ VI) of the CIE. During the trough-shaped CIE segment and between peaks b and c, conifer forests were replaced by more diverse, angiosperm-rich vegetation with increased contents of Normapolles-derived pollen (AZ III and V). Late Cenomanian taxa assigned to Atlantopollis and Complexiopollis are the first representatives of the Normapolles complex36,43, an angiosperm group, which dominated mid-latitude northern hemisphere assemblages during the Late Cretaceous and Early Cenozoic. Based on in-situ findings in fossil flowers, pollen of the Normapolles-type is related to core Fagales44. The thick, often multi-layered exine and complex apertures indicate anemophily45 and are considered adaptions to open vegetation with widely spaced trees under more dry to seasonally dry climates46. During the late Cenomanian, Normapolles-producing angiosperms were probably small non-woody plants or shrubs forming part of a xerophytic savanna-type vegetation47,48—a view supported by the rarity of fossil dicot wood in Cenomanian mid-latitude strata from Europe49. Accordingly, the palynological record across OAE2 shows changing proportion of arborescent conifer forests (reflecting more mesic conditions) and more open, non-arborescent, angiosperm-rich vegetation.

Fluctuations in the overall climatic patterns during OAE2 have been reported earlier based on marine-derived proxy data. Exceptional climatic warmth associated with OAE2 is considered to have caused accelerated hydrological cycling, enhanced weathering and a generally more humid climate9,50,51,52. Phases of enhanced moisture availability may have fostered the spread of mesic conifer-dominated forest ecosystems during the onset and later phase of OAE2. Such warm and humid conditions were punctuated by a series of pronounced climatic coolings during the so-called Plenus Cold Event, PCE53,54. The PCE represents a phase of climatic instability and is characterized by several short-lasting SST drops and increases in the range of 2.5–11 °C5,6,7,8,9,10,11,12,13 and paralleled by the southward migration of boreal fauna55. Climatic instability was accompanied by a shift towards significantly drier conditions in northern hemisphere mid-latitudes9. Stratigraphically, the main pulse of the PCE is located above the first CIE build-up (peak a) at Eastbourne54, where it corresponds approximately to the boundary between the R. cushmani and W. archaeocretacea zones and UC3 to UC4 transition, respectively56. At Cassis, the PCE is expressed in a series of several transient drops of TEX86-derived SSTs below 32 °C with the strongest SST decline occurring within the upper part of the CIE trough interval (Fig. 3), similar to what has been observed elsewhere5. This part of the CIE with a shift towards lower δ13C values has been related to improved bottom-water oxygenation, enhanced organic carbon remineralization and significant fluctuations in atmospheric pCO213,54,57,58. In continental mid-latitude settings such as Cassis, this phase of climatic upheaval is characterized by the proliferation of open, savanna-type vegetation rich in angiosperms at the expanse of conifer-dominated forest ecosystems (Fig. 4). Once established, the savanna-type biome was able to persist even during recurrent phases of exceptional warmth in the course of the PCE.

Fig. 4

Tentative changes in mid-latitude vegetation patterns during OAE2. During OAE mode A (e.g. represented by AZ II, IV and VI), the prevailing climate was characterized by exceptional warmth and high moisture availability, giving way to conifer-dominated forests with moderate angiosperm contribution. During OAE mode B (AZ III and V), climatic conditions were cooler and less humid resulting in an open, savanna-type vegetation community with increased abundances of Normapolles-producing angiosperms. (a) Araucariaceae, (b) other conifers incl. Cheirolepidiaceae, (c) Cupressaceae, (d) angiosperms incl. Normapolles-producing forms, (e) ferns

The onset of the Cretaceous thermal maximum including OAE2 took place against the background of a major turnover in global land plant vegetation, namely the rise of angiosperms towards ecological dominance. In mid-latitude settings of North America and Europe, this floral change is marked by the Late Cenomanian radiation of Normapolles-producing plants related to core Fagales43,45. In the Cassis record, early representatives of this group show a pronounced increase in the uppermost Cenomanian assemblage zone III, subsequent to their Mid- to Late Cenomanian origination36. Within the overall warm and humid greenhouse conditions characterizing OAE2, a transient shift towards relatively drier climates and punctuated cooling during the PCE may have fostered a first spread of Normapolles-type angiosperms, which henceforward became a very diverse and successful group dominating mid-latitude plant ecosystems throughout the Late Cretaceous to Early Cenozoic for more than ~50 Ma.


Stable isotope analyses of carbonate and organic carbon

Measurements of stable carbon and oxygen isotopes of sedimentary carbonates were carried out on powdered bulk rock material (~0.5 mg) on a total of 292 samples. Stable isotope analysis was conducted using a Thermo Fisher Scientific Gasbench II carbonate device connected to a Thermo Fisher Scientific Delta V Advantage IRMS, available at the Leibniz University Hannover, Germany. The gas bench uses viscous water-free (98 g/mol) orthophosphoric acid at 72 °C to release CO2 of the calcite from the sample material 1 h before the start of the measurement. Repeated analyses of certified carbonate standards (CO-1, NBS-18, NBS-19) show an external reproducibility ± 0.08‰ for δ18O and ± 0.06‰ for δ13Ccarb. Values are expressed in conventional delta notation relative to the Vienna-Pee Dee Formation belemnite (VPDB) international standard, in per mil (‰) Stable carbon isotope analyses of bulk organic carbon (δ13Corg) were performed on 117 decarbonated samples. Powdered samples were treated twice with 6 M HCl for 12 h to remove any carbonate phases and rinsed subsequently with deionised H2O until neutrality was reached. Stable carbon isotope composition of bulk Corg was determined using an organic elemental analyser (Thermo Scientific Flash 2000) connected online to a Thermo Fisher Scientific Delta V Advantage IRMS, available at the Leibniz University Hannover, Germany. The analytical accuracy and reproducibility is checked by replicate analyses of international standards (NBS 22). Reproducibility was better than ±0.1‰ for δ13Corg. Values are expressed in conventional delta notation relative to the Vienna-Pee Dee Formation belemnite (VPDB) international standard, in per mil (‰).


A total of 67 rock samples from the Cassis section were prepared for palynological analysis by the Geological Survey of North Rhine-Westphalia in Krefeld, Germany. Cleaned, crushed and weighed samples (20 to 50 g) were treated with 30% HCl and 38% HF for carbonate and silica removal, respectively. Residues were sieved over a 11-μm mesh and mounted on microscope slides, which were analyzed at ×200 and ×1000 magnification. All samples were productive and studied for their particle content (palynofacies) and sporomorph assemblage (spores and pollen), respectively. For the quantification of the spore-pollen assemblage, a minimum of 250 grains were determined per slide (avg. 272 grains) and one entire slide was scanned for rare elements. Five samples did not provide enough sporomorphs to reach the target count of 250 grains. Variations in the spore-pollen assemblage represent normalized frequencies and are reported in percentage [%] of the total assemblage. Thermally unaltered preservation of organic matter is indicated by the virtually unchanged coloring of the sporomorphs and shows a thermal alteration index (TAI) < 259. Preservation of the individual pollen grains varies from moderate to good. Sporomorphs are assigned to floral groups according to their botanical affinity60,61.

Biomarker analysis

For TEX86 analysis, a total of 69 powdered and freeze dried samples (5–10 g dry mass) were extracted with an accelerated solvent extractor, using a 9:1 (v/v) dichlormethane (DCM):MeOH solvent mixture, 3 times for 5 min. at a pressure of ca. 7.6 × 106 Pa and a temperature of 100 °C. The obtained total extracts were rotary evaporated and separated over an activated Al2O3 column using 9:1 (v/v) hexane:DCM and 1:1 (v/v) DCM:MeOH solvent mixtures into an apolar and polar fraction, respectively. The polar fraction, containing the glycerol dialkyl glycerol tetraether lipids (GDGTs), was dried under a pure N2 flow, dissolved ultrasonically in a 99:1 (v/v) hexane:isopropanol mixture at a concentration of 2 mg/ml and filtered over an 0.45 μm mesh PTFE filter (Ø 4 mm) prior to HPLC/MS analysis. High-performance liquid chromatography/atmospheric pressure chemical ionization mass spectrometry (HPLC/APCI-MS) analyses was be performed on an Agilent 1100 series/Hewlett-Packard 1100 MSD series machine equipped with an auto-injector and HP Chemostation software following62.

GDGTs were quantified by integration of peak areas and the TetraEther indeX of tetraethers composed of 86 carbon atoms (TEX86) was determined63. In order to assess the influence of soil-derived GDGTs on TEX86 values, the BIT index64 was applied. Samples with BIT index > 0.3 were excluded from SST reconstruction65. Absolute SSTs were reconstructed for 64 samples using TEX86H core top calibration equations66, which has a calibration error of 2.5 °C. The analytical error of TEX86H-based SST estimates was 0.07 °C based on duplicate analysis. We used the TEX86H calibration rather than other calibrations67 in order to remain consistent with previous literature6 and as this has recently been shown to match independent temperature estimates in tropical regions during the Eocene hothouse, the warmest period in the Cenozoic68. Although the uncertainty of the calibration used is 2.5 °C, comparisons with other proxy datasets6 suggests that TEX86 sometimes can overestimate SSTs, or have a seasonal bias, e.g., toward summer temperatures. Nevertheless, even considering this, the here presented SST estimates of up to 38 °C do suggest hot tropical temperatures well above 30 °C. A level-by-level comparison of TEX86 values and G/A-ratios based on 42 samples supports a general link between SSTs and gross vegetation patterns (Supplementary Fig. 3).

For compound-specific carbon isotope measurements, apolar fractions were treated using an Ag-Silica column with hexane and subsequently ethyl acetate to gain a mostly n-alkane pure fraction, which was evaporated under N2 stream followed by dissolution in 25–50 µl hexane. For measuring the δ13C composition of individual n-alkanes, 1 ml was injected into the gas chromatograph isotope ratio mass spectrometer (Agilent 6890N GC coupled to a Thermo Delta V advantage IRMS), equipped with a fuse silica capillary column coated with CP-Sil5, with helium used as a carrier gas. The oven was programmed at a starting (injection) temperature of 70 °C, which rose to 130 °C at 20°/min and then 320° at 4°/min, at which it was maintained for 20 min. Values are expressed in conventional delta notation relative to the Vienna-Pee Dee Formation belemnite (VPDB) international standard, in per mil (‰). All biomarker analyses were carried out at the NIOZ (Royal Netherlands Institute of Sea Research, The Netherlands).

Data availability

All data generated and/or analyzed in this study are included in this published article and its supplementary information file, and are also available from the corresponding author on reasonable request.


  1. 1.

    Jaramillo, C. et al. Effects of rapid global warming at the Paleocene–Eocene boundary on neotropical vegetation. Science 330, 957–961 (2010).

    ADS  CAS  Article  PubMed Central  Google Scholar 

  2. 2.

    McElwain, J., Wade-Murphy, J. & Hesselbo, S. P. Changes in carbon dioxide during an oceanic anoxic event linked to intrusion into Gondwana coals. Nature 435, 479–482 (2005).

    ADS  CAS  Article  PubMed Central  Google Scholar 

  3. 3.

    Hochuli, P. A., Sanson-Barrera, A., Schneebeli-Hermann, E. & Bucher, H. Severest crisis overlooked - Worst disruption of terrestrial environments postdates the Permian–Triassic mass extinction. Sci. Rep. 6, 1–7 (2016).

    Article  Google Scholar 

  4. 4.

    Norris, R. D., Bice, K. L., Magno, E. A. & Wilson, P. A. Jiggling the tropical thermostat in the Cretaceous hothouse. Geology 30, 299–302 (2002).

    ADS  Article  Google Scholar 

  5. 5.

    Forster, A., Schouten, S., Moriya, K., Wilson, P. A. & Sinninghe Damsté, J. S. Tropical warming and intermittent cooling during the Cenomanian/Turonian Oceanic Anoxic Event 2: Sea surface temperature records from the equatorial Atlantic. Paleoceanography 22, PA1219 (2007).

    ADS  Article  Google Scholar 

  6. 6.

    O’Brien, C. L. et al. Cretaceous sea-surface temperature evolution: constraints from TEX86 and planktonic foraminiferal oxygen isotopes. Earth Sci. Rev. 172, 224–247 (2017).

    Article  Google Scholar 

  7. 7.

    Voigt, S., Gale, A. S. & Flögel, S. Midlatitude shelf seas in the Cenomanian–Turonian greenhouse world: Temperature evolution and North Atlantic circulation. Paleoceanography 19, PA4020 (2004).

    ADS  Article  Google Scholar 

  8. 8.

    Sinninghe Damsté, J. S., Van Bentum, E. C., Reichart, G.-J., Pross, J. & Schouten, S. A CO2 decrease-driven cooling and increased latitudinal temperature gradient during the mid-Cretaceous Oceanic Anoxic Event 2. Earth. Planet. Sci. Lett. 293, 97–103 (2010).

    ADS  Article  Google Scholar 

  9. 9.

    Van Helmond, Na. G. M. et al. A perturbed hydrological cycle during Oceanic Anoxic Event 2. Geology 42, 123–126 (2014).

    ADS  Article  Google Scholar 

  10. 10.

    Eldrett, J. S. et al. An astronomically calibrated stratigraphy of the Cenomanian, Turonian and earliest Coniacian from the Cretaceous Western Interior Seaway, USA: implications for global chronostratigraphy. Cretac. Res. 56, 316–344 (2015).

    Article  Google Scholar 

  11. 11.

    Li, Y.-X., Montañez, I. P., Liu, Z. & Ma, L. Astronomical constraints on global carbon-cycle perturbation during Oceanic Anoxic Event 2 (OAE2). Earth. Planet. Sci. Lett. 462, 35–46 (2017).

    ADS  CAS  Article  Google Scholar 

  12. 12.

    Schlanger, S. O., Arthur, M. A., Jenkyns, H. C. & Scholle, P. A. The Cenomanian–Turonian Oceanic Anoxic Event, I. Stratigraphy and distribution of organic carbon-rich beds and the marine δ13C excursion. Geol. Soc. Lond. Spec. Publ. 26, 371–399 (1987).

    ADS  Article  Google Scholar 

  13. 13.

    Jarvis, I., Lignum, J. S., Gröcke, D. R., Jenkyns, H. C. & Pearce, M. A. Black shale deposition, atmospheric CO2 drawdown, and cooling during the Cenomanian–Turonian Oceanic Anoxic Event. Paleoceanography 26, PA3201 (2011).

    ADS  Article  Google Scholar 

  14. 14.

    Arthur, M. A., Dean, W. E. & Pratt, L. M. Geochemical and climatic effects of increased marine organic carbon burial at the Cenomanian/Turonian boundary. Nature 335, 714–717 (1988).

    ADS  Article  Google Scholar 

  15. 15.

    Tsikos, H. et al. Carbon-isotope stratigraphy recorded by the Cenomanian–Turonian Oceanic Anoxic Event: correlation and implications based on three key localities. J. Geol. Soc. Lond. 161, 711–719 (2004).

    CAS  Article  Google Scholar 

  16. 16.

    Fischer, V., Bardet, N., Benson, R. B. J., Arkhangelsky, M. S. & Friedman, M. Extinction of fish-shaped marine reptiles associated with reduced evolutionary rates and global environmental volatility. Nat. Commun. 7, 1–11 (2016).

    Google Scholar 

  17. 17.

    Monnet, C. The Cenomanian–Turonian boundary mass extinction (late Cretaceous): new insights from ammonoid biodiversity patterns of Europe, Tunisia and the Western Interior (North America). Palaeogeog. Palaeoclim. Palaeoecol. 282, 88–104 (2009).

    Article  Google Scholar 

  18. 18.

    Jenkyns, H. C. Geochemistry of oceanic anoxic events. Geochem. Geophys 11, Q03004 (2010).

    Google Scholar 

  19. 19.

    Gomez, B. et al. Cretaceous conifers and angiosperms from the Bonarelli Level; reassessment of Massalongo’s plant fossil collections of “Monte Colle”, Lessini Mountains, northern Italy. Cretac. Res. 52, 179–193 (2015).

    Article  Google Scholar 

  20. 20.

    Kuypers, M. M. M., Pancost, R. D. & Sinninghe Damsté, J. A large and abrupt fall in atmospheric CO2 concentration during Cretaceous times. Nature 399, 342–345 (1999).

    ADS  CAS  Article  Google Scholar 

  21. 21.

    Hay, W. W. & Flögel, S. New thoughts about the Cretaceous climate and oceans. Earth Sci. Rev. 115, 262–272 (2012).

    ADS  CAS  Article  Google Scholar 

  22. 22.

    Jolet, P., Philip, J., Thomel, G., López, G. & Tronchetti, G. Nouvelles données biostratigraphiques sur la limite Cénomanien–Turonien. La coupe de Cassis (Sud-Est de la France): Proposition d’un hypostratotype européen. Geobios 34, 225–238 (2001).

    Article  Google Scholar 

  23. 23.

    Paul, C. R. C. et al. The Cenomanian–Turonian boundary at Eastbourne (Sussex, UK): a proposed European reference section. Palaeogeog. Palaeoclim. Palaeoecol. 150, 83–121 (1999).

    ADS  Article  Google Scholar 

  24. 24.

    Jarvis, I., Gale, A. S., Jenkyns, H. C. & Pearce, M. A. Secular variations in late Cretaceous carbon isotopes: a new δ13C carbonate reference curve for the Cenomanian–Campanian (99.6–70.6 Ma). Geol. Mag. 143, 561–608 (2006).

    ADS  CAS  Article  Google Scholar 

  25. 25.

    Floquet, M., Léonide, P., Villier, L., Ackouala, A. P., Blenet, A. Expressions biosédimentaire, diagénétique, géochimique et tectonique de l’événement anoxique Cénomano-Turonien (OAE 2) par les plates-formes carbonatées sud-provençales. sumé de communication, 13ème Congrès Français de Sédimentologie, Paris (2013).

  26. 26.

    Peyrot, D., Barroso-Barcenilla, F. & Feist-Burkhardt, S. Palaeoenvironmental controls on late Cenomanian–early Turonian dinoflagellate cyst assemblages from Condemios (Central Spain). Rev. Palaeobot. Palynol. 180, 25–40 (2012).

    Article  Google Scholar 

  27. 27.

    Swart, P. K. & Eberli, G. The nature of the δ13C of periplatform sediments: Implications for stratigraphy and the global carbon cycle. Sed. Geol. 175, 115–129 (2005).

    CAS  Article  Google Scholar 

  28. 28.

    Floquet, M., Gari, J., Hennuy, J., Léonide, P., Philip, J. Sédimentations gravitaires carbonatées et silicoclastiques dans un bassin en transtension, séries d′âge Cénomanien à Coniacien moyen du Bassin Sud-Provençal. Field guide of the 10 ème Congrès Francais de Sédimentologie, 1–80 (2005).

  29. 29.

    Herngreen, G. F. W., Kedves, M., Rovina, L. V., Smirnova, S. B. in Palynology: Principles and Applications Vol. 3 (eds Jansonius, J. & McGregor, D. C.) 1157–1188 (AASP Foundation, 1996).

  30. 30.

    Sun, Y. et al. Lethally hot temperatures during the early Triassic greenhouse. Science 338, 366–370 (2012).

    ADS  CAS  Article  PubMed Central  Google Scholar 

  31. 31.

    Cascales-Miñana, B. & Cleal, C. J. The plant fossil record reflects just two great extinction events. Terra Nova 26, 195–200 (2014).

    ADS  Article  Google Scholar 

  32. 32.

    Romano, C. et al. Climatic and biotic upheavals following the end-Permian mass extinction. Nat. Geosci. 6, 57–60 (2013).

    ADS  CAS  Article  Google Scholar 

  33. 33.

    Hermann, E. et al. Terrestrial ecosystems on North Gondwana following the end-Permian mass extinction. Gondwana Res. 20, 630–637 (2011).

    ADS  Article  Google Scholar 

  34. 34.

    Berry, J. & Björkman, O. Photosynthetic response and adaption to temperature in higher plants. Annu. Rev. Plant. Physiol. 31, 491–543 (1980).

    Article  Google Scholar 

  35. 35.

    Huber, M. A hotter greenhouse? Science 321, 353–354 (2008).

    CAS  Article  PubMed Central  Google Scholar 

  36. 36.

    Méon, H., Guignard, G., Pacltová, B. & Svobodová, M. Normapolles. Comparison between central and southwestern Europe during the Cenomanian and Turonian: Evolution of biodiversity and paleoenvironment. Bull. Soc. Geol. Fr. 175, 579–593 (2004).

    Article  Google Scholar 

  37. 37.

    Peyrot, D., Barrón, E., Comas-Rengifo, M. J., Barroso-Barcenilla, F. & Feist-Burkhardt, S. Palynological characterization of the Cenomanian/Turonian boundary at Puentedey (Burgos, Spain). Coloq. Pal 58, 101–161 (2008).

    Google Scholar 

  38. 38.

    Poulsen, C. J., Tabor, C. & White, J. D. Long-term climate forcing by atmospheric oxygen concentrations. Science 348, 1238–1241 (2015).

    ADS  CAS  Article  PubMed Central  Google Scholar 

  39. 39.

    Schrank, E. Pollen and spores from the Tendaguru beds, upper Jurassic and lower Cretaceous of southeast Tanzania: palynostratigraphical and paleoecological implications. Palynology 34, 3–42 (2010).

    Article  Google Scholar 

  40. 40.

    Kershaw, P. & Wagstaff, B. The southern conifer family Araucariaceae: History, status, and value for paleoenvironmental reconstruction. Annu. Rev. Ecol. Syst. 32, 397–414 (2001).

    Article  Google Scholar 

  41. 41.

    Peralta-Medina, E. & Falcon-Lang, H. J. Cretaceous forest composition and productivity inferred from a global fossil wood database. Geology 40, 219–222 (2012).

    ADS  Article  Google Scholar 

  42. 42.

    Kunzmann, L. Araucariaceae (Pinopsida): aspects in palaeobiogeography and palaeobiodiversity in the Mesozoic. Zool. Anz. 246, 257–277 (2007).

    Article  Google Scholar 

  43. 43.

    Batten, D. J. Stratigraphic, palaeogeographic and evolutionary significance of late Cretaceous and early Tertiary Normapolles pollen. Rev. Palaeobot. Palynol. 35, 125–137 (1981).

    Article  Google Scholar 

  44. 44.

    Friis, E. M., Pedersen, K. R. & Schönenberger, J. Normapolles plants: a prominent component of the Cretaceous rosid diversification. Plant Syst. Evol. 260, 107–140 (2006).

    Google Scholar 

  45. 45.

    Friis, E. M., Crane, P. R. & Pedersen, K. R. Early Flowers and Angiosperm Evolution (Cambridge Univ. Press, Cambridge, 2011).

    Book  Google Scholar 

  46. 46.

    Wolfe, J. A. & Upchurch, G. R. North American nonmarine climates and vegetation during the late Cretaceous. Palaeogeog. Palaeoclim. Palaeoecol. 61, 33–77 (1987).

    ADS  Article  Google Scholar 

  47. 47.

    Wing, S. L. & Tiffney, B. H. The reciprocal interaction of angiosperm evolution and tetrapod herbivory. Rev. Palaeobot. Palynol. 50, 179–210 (1987).

    Article  Google Scholar 

  48. 48.

    Sewall, J. O. et al. Climate model boundary conditions for four Cretaceous time slices. Clim. Past. 3, 647–657 (2007).

    Article  Google Scholar 

  49. 49.

    Philippe, M. et al. Woody or not woody? Evidence for early angiosperm habit from the early Cretaceous fossil wood record of Europe. Palaeoworld 17, 142–152 (2008).

    Article  Google Scholar 

  50. 50.

    Scopelliti, G. et al. High-resolution geochemical and biotic records of the Tethyan ‘Bonarelli Level’ (OAE2, latest Cenomanian) from the Calabianca-Guidaloca composite section, northwestern Sicily, Italy. Palaeogeog. Palaeoclim. Palaeoecol. 208, 293–317 (2004).

    Article  Google Scholar 

  51. 51.

    Pogge Von, Strandmann, P. A., E., Jenkyns, H. C. & Woodfine, R. G. Lithium isotope evidence for enhanced weathering during Oceanic Anoxic Event 2. Nat. Geosci. 6, 668–672 (2013).

    ADS  Article  Google Scholar 

  52. 52.

    Van Helmond, N. A. G. M. et al. Freshwater discharge controlled deposition of Cenomanian–Turonian black shales on the NW European epicontinental shelf (Wunstorf, northern Germany). Clim. Past. 11, 495–508 (2015).

    Article  Google Scholar 

  53. 53.

    Gale, A. S. & Christensen, W. K. Occurrence of the belemnite Actinocamax plenus in the Cenomanian of SE France and its significance. Bull. Geol. Soc. Den. 43, 68–77 (1996).

    Google Scholar 

  54. 54.

    Jenkyns, H. C., Dickson, A. J., Ruhl, M. & Van Den Boorn, S. H. J. M. Basalt-seawater interaction, the Plenus Cold Event, enhanced weathering and geochemical change: deconstructing Oceanic Anoxic Event 2 (Cenomanian–Turonian, late Cretaceous). Sedimentology 64, 16–43 (2017).

    CAS  Article  Google Scholar 

  55. 55.

    Van Helmond, N. A. G. M. et al. Equatorward phytoplankton migration during a cold spell within the late Cretaceous super-greenhouse. Biogeosciences 13, 2859–2872 (2016).

    ADS  Article  Google Scholar 

  56. 56.

    Linnert, C., Mutterlose, J. & Mortimore, R. Calcareous nannofossils from Eastbourne (southeastern England) and the paleoceanography of the Cenomanian–Turonian boundary interval. Palaios 26, 298–313 (2011).

    ADS  Article  Google Scholar 

  57. 57.

    Eldrett, J. S., Minisini, D. & Bergman, S. C. Decoupling of the carbon cycle during Ocean Anoxic Event 2. Geology 42, 567–570 (2014).

    ADS  CAS  Article  Google Scholar 

  58. 58.

    Barclay, R. S., McElwain, J. C. & Sageman, B. B. Carbon sequestration activated by a volcanic CO2 pulse during Ocean Anoxic Event 2. Nat. Geosci. 3, 205–208 (2010).

    ADS  CAS  Article  Google Scholar 

  59. 59.

    Staplin, F. L. in How to Assess Maturation and Palaeotemperatures, SEPM Short Course 7 (ed Staplin, F. L.) 7–31 (Society of Economic Paleontologists and Mineralogists, 1982).

  60. 60.

    Balme, B. E. Fossil in situ spores and pollen grains: an annotated catalogue. Rev. Palaeobot. Palynol. 87, 81–323 (1995).

    Article  Google Scholar 

  61. 61.

    Abbink, O. A., Van Konijnenburg - Van Cittert, J. H. A. & Visscher, H. A sporomorph ecogroup model for the northwest European Jurassic–lower Cretaceous: concepts and framework. Geol. Mijnb. 83, 17–31 (2004).

    Article  Google Scholar 

  62. 62.

    Schouten, S., Huguet, C., Hopmans, E. C., Kienhuis, M. V. M. & Sinninghe Damsté, J. S. Analytical methodology for TEX86 paleothermometry by high-performance liquid chromatography/atmospheric pressure chemical ionization-mass spectrometry. Anal. Chem. 79, 2940–2944 (2007).

    CAS  Article  PubMed Central  Google Scholar 

  63. 63.

    Schouten, S., Hopmans, E. C., Schefuß, E. & Sinninghe Damsté, J. S. Distributional variations in marine crenarchaeotal membrane lipids: a new tool for reconstructing ancient sea water temperatures? Earth. Planet. Sci. Lett. 204, 265–274 (2002).

    ADS  CAS  Article  Google Scholar 

  64. 64.

    Hopmans, E. C., Weijers, J. W. H., Schefuß, E., Herfort, L. & Sinninghe Damsté, J. S. A novel proxy for terrestrial organic matter in sediments based on branched and isoprenoid tetraether lipids. Earth. Planet. Sci. Lett. 224, 107–116 (2004).

    ADS  CAS  Article  Google Scholar 

  65. 65.

    Weijers, J. W. H., Schouten, S., Spaargaren, O. C. & Sinninghe Damsté, J. S. Occurrence and distribution of tetraether membrane lipids in soils: Implications for the use of the TEX86 proxy and the BIT index. Org. Geochem. 37, 1680–1693 (2006).

    CAS  Article  Google Scholar 

  66. 66.

    Kim, J. H. et al. New indices for calibrating the relationship of the distribution of archaeal isoprenoid tetraether lipids with sea surface temperature. Geochim. Cosmochim. Acta 74, 4639–4654 (2010).

    ADS  CAS  Article  Google Scholar 

  67. 67.

    Tierney, J. E. & Tingley, M. P. A Bayesian, spatially-varying calibration model for the TEX86 proxy. Geochim. Cosmochim. Acta 127, 83–106 (2014).

    ADS  CAS  Article  Google Scholar 

  68. 68.

    Evans, D. et al. Eocene greenhouse climate revealed by coupled clumped isotope-Mg/Ca thermometry. Proc. Natl Acad. Sci. USA 115, 1174–1179 (2018).

    ADS  Article  PubMed Central  Google Scholar 

  69. 69.

    Keller, G., Han, Q., Adatte, T. & Burns, S. J. Palaeoenvironment of the Cenomanian–Turonian transition at Eastbourne, England. Cretac. Res. 22, 391–422 (2001).

    Article  Google Scholar 

  70. 70.

    Voigt, S., Gale, A. S. & Voigt, T. Sea-level change, carbon cycling and palaeoclimate during the late Cenomanian of northwest Europe; an integrated palaeoenvironmental analysis. Cretac. Res. 27, 836–858 (2006).

    Article  Google Scholar 

Download references


This study was supported by DFG grant HE4467/4-1 and 4-2 to U.H. S.S. was supported by the Netherlands Earth System Science Center funded by the Dutch Ministry of Education, Culture and Science. We gratefully acknowledge Marc Floquet, Katharina Müller, Jean Cors, Pauline Rais, and Alexander Brandt for their assistance during field work in SE France and Christiane Wenske for analytical support. We thank Stefan Huck for comments on an earlier version of the manuscript.

Author information




U.H. and T.A. conceived and designed the project with input from S.S. U.H. and T.A. collected the rock samples used in this study. N.W. and U.H. analyzed the palynomorphs with input from E.S.-H. S.G. and G.K. established the biostratigraphy, S.K. carried out the stable isotope measurements. A.K. carried out the biomarker analyses with the assistance of S.S. U.H. wrote the manuscript with input from all authors.

Corresponding author

Correspondence to Ulrich Heimhofer.

Ethics declarations

Competing interests

The authors declare no competing interests

Additional information

Publisher's note: Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

Electronic supplementary material

Rights and permissions

Open Access This article is licensed under a Creative Commons Attribution 4.0 International License, which permits use, sharing, adaptation, distribution and reproduction in any medium or format, as long as you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made. The images or other third party material in this article are included in the article’s Creative Commons license, unless indicated otherwise in a credit line to the material. If material is not included in the article’s Creative Commons license and your intended use is not permitted by statutory regulation or exceeds the permitted use, you will need to obtain permission directly from the copyright holder. To view a copy of this license, visit

Reprints and Permissions

About this article

Verify currency and authenticity via CrossMark

Cite this article

Heimhofer, U., Wucherpfennig, N., Adatte, T. et al. Vegetation response to exceptional global warmth during Oceanic Anoxic Event 2. Nat Commun 9, 3832 (2018).

Download citation

Further reading


By submitting a comment you agree to abide by our Terms and Community Guidelines. If you find something abusive or that does not comply with our terms or guidelines please flag it as inappropriate.


Quick links