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Terrestrial Cooling in Northern Europe During the Eocene–Oligocene Transition

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Terrestrial Cooling in Northern Europe During the Eocene–Oligocene Transition Terrestrial cooling in Northern Europe during the Eocene–Oligocene transition Michael T. Hrena,b,1, Nathan D. Sheldonc, Stephen T. Grimesd, Margaret E. Collinsone, Jerry J. Hookerf, Melanie Buglerd, and Kyger C. Lohmannc aDepartment of Chemistry and bCenter for Integrative Geoscience, University of Connecticut, Storrs, CT 06269; cDepartment of Earth and Environmental Sciences, University of Michigan, Ann Arbor, MI 48109; dSchool of Geography, Earth and Environmental Sciences, University of Plymouth, Plymouth, Devon PL4 8AA, United Kingdom; eDepartment of Earth Sciences, Royal Holloway University of London, Egham, Surrey TW20 0EX, United Kingdom; and fDepartment of Palaeontology, Natural History Museum, London SW7 5BD, United Kingdom Edited by Thure E. Cerling, University of Utah, Salt Lake City, UT, and approved March 20, 2013 (received for review June 27, 2012) Geochemical and modeling studies suggest that the transition from heterogeneous climate responses. Some records show no major the “greenhouse” state of the Late Eocene to the “icehouse” condi- climatic changes during the EOT glaciation (6, 10) and others tions of the Oligocene 34–33.5 Ma was triggered by a reduction of show cooling of 8 °C (11), increased seasonality (9, 12), and ari- atmospheric pCO2 that enabled the rapid buildup of a permanent ice dification (13). This discrepancy confounds efforts to determine sheet on the Antarctic continent. Marine records show that the drop the timescale and sensitivity of terrestrial climate response to p fi in CO2 during this interval was accompanied by a signi cant decline changing atmospheric pCO2 or ocean circulation. We measure 18 in high-latitude sea surface and deep ocean temperature and en- the δ OandΔ47 of CO2 derived from carbonate shells of the hanced seasonality in middle and high latitudes. However, terrestrial freshwater gastropod Viviparus lentus from the Hampshire Basin, records of this climate transition show heterogeneous responses to United Kingdom. (Fig. S1). Our results provide unique constraints p changing CO2 and ocean temperatures, with some records showing on Northern Hemisphere terrestrial paleoclimate change during fi p asigni cant time lag in the temperature response to declining CO2. the EOT and indicate cooling of ∼4–6°Cinmeanannualairtem- Δ We measured the 47 of aragonite shells of the freshwater gastro- peratures (MAAT) in northern Europe in response to atmospheric pod Viviparus lentus from the Solent Group, Hampshire Basin, CO2 reductions and Antarctic glaciation. United Kingdom, to reconstruct terrestrial temperature and hydro- logic change in the North Atlantic region during the Eocene–Oligocene Results and Discussion transition. Our data show a decrease in growing-season surface Solent Group Stratigraphy and Paleoclimate. Terrestrial records of water temperatures (∼10 °C) during the Eocene–Oligocene transi- Late Eocene European climate are rare; however, continental tion, corresponding to an average decrease in mean annual air tem- sediments of the Solent Group in the Hampshire Basin (Isle of ∼ – perature of 4 6 °C from the Late Eocene to Early Oligocene. The Wight, United Kingdom) provide an age-calibrated (SI Methods) magnitude of cooling is similar to observed decreases in North At- terrestrial EOT record from the mid-North Atlantic region. lantic sea surface temperature over this interval and occurs during Sediments of the Solent Group were deposited in a coastal plain major glacial expansion. This suggests a close linkage between at- setting at ∼45–50°N from the Late Eocene through the Early mospheric carbon dioxide concentrations, Northern Hemisphere Oligocene and have never been deeply buried, and nearly all temperature, and expansion of the Antarctic ice sheets. remain unlithified (14). Throughout the sequence, freshwater lacustrine and alluvial sediments are punctuated by a few brief clumped isotopes | paleoclimate marine incursions that help provide age control (15). Fossils from the Hampshire Basin indicate a warm Late Eocene he Eocene–Oligocene transition 34–33.5 Ma represents one of climate with abundant marsh vegetation, palms, fruit-eating Tthe most dramatic climatic changes of the past 65 My (1–3). mammals, and crocodilians (14–17). δ18O of carbonate from p Studies suggest that by 34 Ma, CO2 reached a critical threshold freshwater gastropods, fossil rodent teeth, and charophytes within where favorable orbital parameters and ocean circulation patterns Solent Group sediments has been interpreted to show peak Late allowed the rapid buildup of Antarctic ice, triggering widespread Eocene freshwater summer temperatures of >30 °C, with only reduction in atmospheric pCO2 and decreases in sea surface and minor reduction in growing season temperature across the EOT deep ocean temperature (4–8). This event is marked by a +1.5‰ (10, 15, 18). However, δ18O-derived temperatures contrast with shift in the oxygen isotope ratios of carbonate from deep-sea North Atlantic SST and paleofloral data (6, 7), which record sig- benthic foraminifera, which reflects both the glaciation of Antarctica nificant temperature decreases across the EOT. These also con- and rapid cooling of the surface and deep ocean (1, 3). tradict δ18O data from North American fossils that show an ∼8°C Marine sediments provide high-resolution records of surface cooling during this same time (11). One complication with con- and deep ocean temperature responses to the Late Eocene de- ventional δ18O temperature interpretations is that they rely on δ18 creases in pCO2 and Antarctic glaciation (7, 8). These show that estimates of the Owater at the time of formation. Changes in the cooling was amplified in high-latitude regions, with a decrease in isotopic composition of precipitation or ambient water (e.g., due sea surface temperature of >5 °C from the Late Eocene to Early to evaporation) can introduce uncertainty in reconstructions of Oligocene (7). Tropical sea surface temperature (SST) and deep ocean records show mixed responses to global cooling across the Δ Eocene–Oligocene transition (EOT), with some indicating only Author contributions: M.T.H. and K.C.L. developed and conducted 47 measurements at the University of Michigan; N.D.S., S.T.G., M.E.C., J.J.H., and M.B. collected samples in the modest declines in temperature in the tropics (8) and others fi – fi eld; M.B. conducted XRD analyses of gastropod shells; S.T.G., M.E.C., and J.J.H. devel- showing a 3 4 °C decrease in SST during the rst stage of the oped chronostratigraphy, regional correlation, and data on fossil biota; and M.T.H., N.D.S., cooling event (EOT-1) (9). One recent multiproxy study suggests S.T.G., M.E.C., J.J.H., M.B., and K.C.L. wrote the paper. that cooling during the EOT was specifically linked to increased The authors declare no conflict of interest. seasonality, with the majority of cooling occurring during the cool- This article is a PNAS Direct Submission. season months (9). 1To whom correspondence should be addressed. E-mail: [email protected]. There are relatively few terrestrial records of the EOT from This article contains supporting information online at www.pnas.org/lookup/suppl/doi:10. the mid- to high latitudes, and terrestrial paleoclimate data show 1073/pnas.1210930110/-/DCSupplemental. 7562–7567 | PNAS | May 7, 2013 | vol. 110 | no. 19 www.pnas.org/cgi/doi/10.1073/pnas.1210930110 Downloaded by guest on September 24, 2021 paleotemperature in the Late Eocene to Early Oligocene of the (PRISM Climate Group). These data show that Δ47 temperatures Hampshire Basin (10). for aquatic gastropods reliably match conventional oxygen isotope paleothermometry estimates when water δ18O is well constrained, “ Clumped Isotope Paleothermometry. The clumped isotope ther- unlike terrestrial gastropod Δ47 temperatures (25). However, mometer” is a temperature proxy based on a measure of the aquatic gastropod Δ data are biased by seasonal temperature 13 47 temperature-dependent abundance of doubly substituted Cand variation during the period of shell growth. 18 O isotopes that are bound to each other within the carbonate Multiple lines of evidence indicate that our Δ data record Δ 47 lattice (19). The 47 of carbonate minerals [a measure of the primary values. First, fossil shells are preserved in clay-rich sedi- 13 18 abundance anomaly of C- O bonds in carbonate-derived CO2 ments, which potentially reduced fluid-flow that could have al- fi Δ = 47 47 − × and de ned as 47 (R actual/R stochastic 1) 1,000] pro- tered the primary shell structure during burial. Second, Solent δ13 δ18 vides a measure of formation temperature, C, and Oofcar- Group sediments have not been deeply buried, heated, or exten- δ18 bonate and allows direct calculation of O of parent water (20). sively altered, and most sediments remain unlithified (14–16, 26). Although low-temperature diagenetic alteration of aragonite to Δ47 Measurements and Data Reduction. We collected shells of the V. lentus fi secondary calcite is commonly observed in the rock record (27), all freshwater prosobranch gastropod from ve localities samples were analyzed by X-ray diffraction and produced patterns within the Solent Group of the Hampshire Basin, Isle of Wight, for δ18 Δ consistent with aragonite (28). Third, thin-section analyses of in- O and 47 temperature measurement. Samples were collected dividual shells showed an outer layer with vertical crystals in all from 10 intervals that span nearly 3 My of the Late Eocene to shells. The prismatic, alternating vertical crystals and clear growth Early Oligocene (Table S1). Sediments were dried, disagregated, cessation marks are consistent with modern Viviparus species (Fig. and sieved to separate shell materials. Shells were embedded in 1andFigs. S2 and S3), indicating preservation of primary struc- epoxy for thin-section analyses (Figs. S2 and S3). For high-reso- ture. Finally, we conducted high-resolution microsampling of five lution δ18O, complete shells were broken into consecutive pieces, pristine shells to examine the variability in δ18O of individual shells and each was supported internally by epoxy and microsampled.
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