The East Antarctic Ice Sheet (EAIS) is the largest potential contributor to sea-level rise. However, efforts to predict the future evolution of the EAIS are hindered by uncertainty in how it responded to past warm periods, for example, during the Pliocene epoch (5.3 to 2.6 million years ago), when atmospheric carbon dioxide concentrations were last higher than 400 parts per million. Geological evidence indicates that some marine-based portions of the EAIS and the West Antarctic Ice Sheet retreated during parts of the Pliocene1,2, but it remains unclear whether ice grounded above sea level also experienced retreat. This uncertainty persists because global sea-level estimates for the Pliocene have large uncertainties and cannot be used to rule out substantial terrestrial ice loss3, and also because direct geological evidence bearing on past ice retreat on land is lacking. Here we show that land-based sectors of the EAIS that drain into the Ross Sea have been stable throughout the past eight million years. We base this conclusion on the extremely low concentrations of cosmogenic 10Be and 26Al isotopes found in quartz sand extracted from a land-proximal marine sediment core. This sediment had been eroded from the continent, and its low levels of cosmogenic nuclides indicate that it experienced only minimal exposure to cosmic radiation, suggesting that the sediment source regions were covered in ice. These findings indicate that atmospheric warming during the past eight million years was insufficient to cause widespread or long-lasting meltback of the EAIS margin onto land. We suggest that variations in Antarctic ice volume in response to the range of global temperatures experienced over this period—up to 2–3 degrees Celsius above preindustrial temperatures4, corresponding to future scenarios involving carbon dioxide concentrations of between 400 and 500 parts per million—were instead driven mostly by the retreat of marine ice margins, in agreement with the latest models5,6.
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Higher than present global mean sea level recorded by an Early Pliocene intertidal unit in Patagonia (Argentina)
Communications Earth & Environment Open Access 23 December 2020
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Naish, T. et al. Obliquity-paced Pliocene West Antarctic ice sheet oscillations. Nature 458, 322–328 (2009).
Cook, C. P. et al. Dynamic behaviour of the East Antarctic ice sheet during Pliocene warmth. Nat. Geosci. 6, 765–769 (2013).
Dutton, A. et al. Sea-level rise due to polar ice-sheet mass loss during past warm periods. Science 349, aaa4019 (2015).
Haywood, A. M., Dowsett, H. J. & Dolan, A. M. Integrating geological archives and climate models for the mid-Pliocene warm period. Nat. Commun. 7, 10646 (2016).
DeConto, R. M. & Pollard, D. Contribution of Antarctica to past and future sea-level rise. Nature 531, 591–597 (2016).
Golledge, N. R. et al. Antarctic climate and ice-sheet configuration during the early Pliocene interglacial at 4.23 Ma. Clim. Past 13, 959–975 (2017).
Barrett, P. J. Resolving views on Antarctic Neogene glacial history—the Sirius debate. Earth Env. Sci. Trans. R. Soc. Edinburgh 104, 31–53 (2013).
Pollard, D. & DeConto, R. M. Modelling West Antarctic ice sheet growth and collapse through the past five million years. Nature 458, 329–332 (2009).
Scherer, R. P., DeConto, R. M., Pollard, D. & Alley, R. B. Windblown Pliocene diatoms and East Antarctic Ice Sheet retreat. Nat. Commun. 7, 12957 (2016).
Kingslake, J., Ely, J. C., Das, I. & Bell, R. E. Widespread movement of meltwater onto and across Antarctic ice shelves. Nature 544, 349–352 (2017).
Raymo, M., Mitrovica, J. X., O’Leary, M. J., DeConto, R. & Hearty, P. Departures from eustasy in Pliocene sea-level records. Nat. Geosci. 4, 328–332 (2011).
Fretwell, P. et al. Bedmap2: improved ice bed, surface and thickness datasets for Antarctica. Cryosphere 7, 375–393 (2013).
Bierman, P. R., Shakun, J. D., Corbett, L. B., Zimmerman, S. R. & Rood, D. H. A persistent and dynamic East Greenland Ice Sheet over the past 7.5 million years. Nature 540, 256–260 (2016).
Gosse, J. C. & Phillips, F. M. Terrestrial in situ cosmogenic nuclides: theory and application. Quat. Sci. Rev. 20, 1475–1560 (2001).
Talarico, F. M., McKay, R. M., Powell, R. D., Sandroni, S. & Naish, T. Late Cenozoic oscillations of Antarctic ice sheets revealed by provenance of basement clasts and grain detrital modes in ANDRILL core AND-1B. Global Planet. Change 96, 23–40 (2012).
Farmer, G. L. & Licht, K. J. Generation and fate of glacial sediments in the central Transantarctic Mountains based on radiogenic isotopes and implications for reconstructing past ice dynamics. Quat. Sci. Rev. 150, 98–109 (2016).
Golledge, N. R. & Levy, R. H. Geometry and dynamics of an East Antarctic Ice Sheet outlet glacier, under past and present climates. J. Geophys. Res. Earth Surf. 116, F03025 (2011).
Jones, R. S. et al. Cosmogenic nuclides constrain surface fluctuations of an East Antarctic outlet glacier since the Pliocene. Earth Planet. Sci. Lett. 480, 75–86 (2017).
Rohling, E. J. et al. Sea-level and deep-sea-temperature variability over the past 5.3 million years. Nature 508, 477–482 (2014); corrigendum 510, 432 (2014).
Snyder, C. W. Evolution of global temperature over the past two million years. Nature 538, 226–228 (2016).
Balco, G., Stone, J. O. & Jennings, C. Dating Plio-Pleistocene glacial sediments using the cosmic-ray-produced radionuclides Be-10 and Al-26. Am. J. Sci. 305, 1–41 (2005).
Rovey, C. W. & Balco, G. Paleoclimatic interpretations of buried paleosols within the pre-Illinoian till sequence in northern Missouri, USA. Palaeogeogr. Palaeoclim. Palaeoecol. 417, 44–56 (2015).
Gasson, E., DeConto, R. M., Pollard, D. & Levy, R. H. Dynamic Antarctic ice sheet during the early to mid-Miocene. Proc. Natl Acad. Sci. USA 113, 3459–3464 (2016).
Winkelmann, R., Levermann, A., Ridgwell, A. & Caldeira, K. Combustion of available fossil fuel resources sufficient to eliminate the Antarctic Ice Sheet. Sci. Adv. 1, e1500589 (2015).
Gulick, S. P. S. et al. Initiation and long-term instability of the East Antarctic Ice Sheet. Nature 552, 225–229 (2017).
Hay, C. et al. The sea-level fingerprints of ice-sheet collapse during interglacial periods. Quat. Sci. Rev. 87, 60–69 (2014).
Wilson, G. S. et al. Neogene tectonic and climatic evolution of the Western Ross Sea, Antarctica—chronology of events from the AND-1B drill hole. Global Planet. Change 96, 189–203 (2012).
Zachos, J., Pagani, M., Sloan, L., Thomas, E. & Billups, K. Trends, rhythms, and aberrations in global climate 65 Ma to present. Science 292, 686–693 (2001).
Lüthi, D. et al. High-resolution carbon dioxide concentration record 650,000–800,000 years before present. Nature 453, 379–382 (2008).
Foster, G. L., Royer, D. L. & Lunt, D. J. Future climate forcing potentially without precedent in the last 420 million years. Nature Comm. 8, 14845 (2017).
Krissek, L. et al. Sedimentology and stratigraphy of the AND-1B core, ANDRILL McMurdo Ice Shelf Project, Antarctica. Terra Antarctica 14, 185–222 (2007).
Corbett, L. B., Bierman, P. R. & Rood, D. H. An approach for optimizing in situ cosmogenic 10Be sample preparation. Quat. Geochronol. 33, 24–34 (2016).
Nishiizumi, K. et al. Absolute calibration of 10Be AMS standards. Nucl. Instrum. Methods Phys. Res. B 258, 403–413 (2007).
Nishiizumi, K. Preparation of 26Al AMS standards. Nucl. Instrum. Methods Phys. Res. B 223–224, 388–392 (2004).
Nuzzo, R. Statistical errors. Nature 506, 150–152 (2014).
Kruschke, J. K. Bayesian estimation supersedes the t test. J. Exp. Psychol. 142, 573–603 (2013).
Kruschke, J. K. Doing Bayesian Data Analysis: A Tutorial with R, JAGS and Stan (Elsevier, London, 2015).
Gelman, A., Carlin, J. B., Stern, H. S. & Rubin, D. B. Bayesian Data Analysis (Chapman & Hall/CRC, London, 2004).
Currie, L. A. The measurement of environmental levels of rare gas nuclides and the treatment of very low-level counting data. IEEE Trans. Nucl. Sci. 19, 119–126 (1972).
Kruschke, J. K. Informed priors for Bayesian comparison of two groups http://doingbayesiandataanalysis.blogspot.com/2015/04/informed-priors-for-bayesian-comparison.html (2015).
R Core Development Team. R: a language and environment for statistical computer http://www.R-project.org/ (2016).
Kruschke, J. K. & Meredith, M. BEST: Bayesian estimation supersedes the t-test https://cran.r-project.org/web/packages/BEST/index.html (2015).
Plummer, M. JAGS: a program for analysis of Bayesian graphical models using Gibbs sampling. In Proc. 3rd Int. Workshop on Distributed Statistical Computing (eds Hornik, K. et al.) (2003).
Plummer, M., Best, N., Cowles, K. & Vines, K. CODA: convergence diagnosis and output analysis for MCMC. R News 6, 7–11 (2006).
Gelman, A. & Rubin, D. B. Inference from iterative simulation using multiple sequences. Stat. Sci. 7, 457–472 (1992).
Korschinek, G. et al. A new value for the half-life of 10Be by heavy-ion elastic recoil detection and liquid scintillation counting. Nucl. Instrum. Methods Phys. Res. B 268, 187–191 (2010).
Norris, T. L., Gancarz, A. J., Rokop, D. J. & Thomas, K. W. Half-life of 26Al. J. Geophys. Res. Solid Earth 88, B331–B333 (1983).
Jamieson, S. S. R., Sugden, D. E. & Hulton, N. R. J. The evolution of the subglacial landscape of Antarctica. Earth Planet. Sci. Lett. 293, 1–27 (2010).
Thomson, S. N., Reiners, P. W., Hemming, S. R. & Gehrels, G. E. The contribution of glacial erosion to shaping the hidden landscape of East Antarctica. Nat. Geosci. 6, 203–207 (2013).
Wellman, P. & Tingey, R. J. Glaciation, erosion and uplift over part of East Antarctica. Nature 291, 142–144 (1981).
Bo, S. et al. The Gamburtsev mountains and the origin and early evolution of the Antarctic Ice Sheet. Nature 459, 690–693 (2009).
Young, D. A. et al. A dynamic early East Antarctic Ice Sheet suggested by ice-covered fjord landscapes. Nature 474, 72–75 (2011).
Heisinger, B. et al. Production of selected cosmogenic radionuclides by muons. Geochim. Cosmochim. Acta 66, A558 (2002).
Balco, G., Stone, J. O., Lifton, N. A. & Dunai, T. J. A complete and easily accessible means of calculating surface exposure ages or erosion rates from 10Be and 26Al measurements. Quat. Geochronol. 3, 174–195 (2008).
Golledge, N. R., Levy, R. H., McKay, R. M. & Naish, T. R. East Antarctic ice sheet most vulnerable to Weddell Sea warming. Geophys. Res. Lett. 44, 2343–2351 (2017).
Peltier, W. R. Global glacial isostasy and the surface of the ice-age Earth: the ICE-5G (VM2) model and GRACE. Annu. Rev. Earth Planet. Sci. 32, 111–149 (2004).
We thank the Antarctic Research Facility for AND-1B samples, and J. X. Mitrovica for his help in performing the glacial isostatic adjustment modelling. This research was supported by National Science Foundation (NSF) grant ARC-1023191 (to P.R.B. and L.B.C.); Boston College start-up funds (to J.D.S.); Vermont Established Program to Stimulate Competitive Research (EPSCoR) grants EPS-1101317 and NSF OIA 1556770 (to K.U. and D.M.R.); NSF grant EAR-1153689 (to M.W.C.); and the New Zealand Ministry of Business Innovation and Employment contract C05X1001 (to T.N. and N.R.G.). This is Lawrence Livermore National Laboratory project LLNL-JRNL-735619.
Nature thanks J. Gosse, E. Gasson, J. Willenbring and the other anonymous reviewer(s) for their contribution to the peer review of this work.
The authors declare no competing interests.
Publisher’s note: Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
Extended data figures and tables
a–d, Simulated erosion potential under the Antarctic Ice Sheet, calculated from modelled driving stress and basal velocity fields for several uniform (atmosphere and ocean) warming scenarios of: 4 °C (a), 8 °C (b), 12 °C (c) and 15 °C (d)55. The location of the AND-1B core is shown by the yellow dot. We note that erosive zones tend to extend towards the continental interior with warming. dT, temperature anomaly from present; dV, ice-volume anomaly from present, in sea-level equivalent (s.l.e.).
a–d, Antarctic land above sea level (yellow) 0 kyr (a), 5 kyr (b), 10 kyr (c), and 15 kyr (d) after a near-instantaneous (1-kyr) collapse of all marine-based ice-sheet sectors, in two different models of mantle viscosity26. Model 1 is from ref. 56, and model 2 (our model) has the following parameters: lithosphere thickness, 96 km; upper-mantle viscosity, 5 × 1020 Pa s−1; and lower-mantle viscosity, 1022 Pa s−1. The location of the AND-1B core is shown by the star.
a, b, Cumulative exceedance probabilities of measured (that is, not blank-corrected) 10Be (a) and 26Al (b) nuclide abundances in AND-1B samples (blue) and in all blanks run by the same operator in the same low-level fume hood (red), with 1σ uncertainties. These plots display the fraction of measurements that exceed a given nuclide abundance. Note that probabilities are generally higher for the samples than the blanks; in other words, a random draw from the samples is more likely to be above a random draw from the blanks, suggesting that they are separable populations.
Shaded intervals surrounding the blue line show 1σ uncertainties, while shaded intervals not surrounding the blue line show the possible range of decay-corrected concentrations in samples that are below the detection limit. The dashed black line simulates the 26Al concentration in non-eroding material at 2,000 metres above sea level (m asl) that was originally saturated at 14 Ma and subsequently decayed under cold-based, non-erosive ice. The fact that several AND-1B samples have higher concentrations than those in this extreme scenario (which is the most favourable to having nuclides persist to the present) suggests that the AND-1B nuclides were produced after the expansion of the EAIS in the mid-Miocene.
Extended Data Fig. 5 Modelled concentrations of cosmogenic nuclides for various durations of interglacial exposure and glacial erosion rates.
a–d, Simulated 10Be (a, b) and 26Al (c, d) concentrations in material sourced from sea level and from 2,000 m asl in Antarctica as a function of the fraction of time for which land is exposed, during 40-kyr glacial cycles. (Results are nearly identical if the cycles are instead 100-kyr long.) Erosion rates were assumed to be 0 m per Myr during ice-free conditions, on the basis of geologic evidence for negligible late Cenozoic erosion in ice-free areas of the TAMs9,10. Black arrows next to the scale bars show the range of decay-corrected nuclide concentrations in AND-1B samples. The model was initialized with zero nuclides at 8 Ma (representative of conditions suggested by AND-1B sample H); the model also assumes instantaneous transport of eroded sediment to the ocean with no mixing, and continuous radioactive decay. Concentrations shown are the Pliocene (5 Ma to 3 Ma) average. Comparison of these simulations with AND-1B nuclide concentrations suggests that land exposure in sediment source regions was probably quite limited in duration or extent through the Plio-Pleistocene.
a–d, Each panel shows actual AND-1B decay-corrected 10Be concentrations with 1σ uncertainty (green), as well as simulated 10Be concentrations assuming a single 10-kyr (a), 50-kyr (b), 100-kyr (c) and 200-kyr (d) exposure of a bedrock column in the mid-Pliocene. The exposure event was chosen to start at 3.6 Ma and extend for up to 200 kyr in duration on the basis of the presence of a 60-m-thick diatomite unit in the AND-1B core, thought to reflect warm interglacial conditions from 3.6 Ma to 3.4 Ma1. Simulated records are driven by production at sea level (grey) or at 2,000 m asl (black), and are subjected to continuous radioactive decay and continuous erosion at rates of 0 m per Myr (solid lines), 20 m per Myr (dashed lines), and 100 m per Myr (dotted lines). The model assumes that the sediment source was initially devoid of nuclides and that sediments are transported instantaneously to the sea floor. The synthetic time series have been binned to the same resolution as the AND-1B data.
Extended Data Fig. 7 Modelling a mid-Pliocene exposure event with eroded bedrock mixed through a deformable bed.
The figure shows AND-1B decay-corrected 10Be concentrations with 1σ uncertainties (green). It also depicts simulated 10Be concentrations, assuming a single exposure event from 3.6 Ma to 3.4 Ma and routing of eroded bedrock through a well mixed deformable bed, for various bed thicknesses and erosion rates. Material eroded from the bedrock profile is instantaneously mixed throughout the deformable bed in each time step, and an equal amount of material is removed from the bed, keeping its thickness constant. Sediment mixing in the deformable bed dilutes the surface 10Be signal of the exposure event but extends its longevity through time in comparison with the bedrock simulations shown in Extended Data Fig. 6. Simulated records are driven by production at sea level, and subjected to continuous radioactive decay and continuous erosion. The model assumes that the bedrock and deformable bed were initially devoid of nuclides and that sediments eroded from the deformable bed are transported instantaneously to the sea floor. The synthetic time series have been binned to the same resolution as the AND-1B data.
Extended Data Fig. 8 Conceptual diagram showing the outcomes of Bayesian one-group t-tests and their interpretation.
a, Nuclides are credibly present above background: that is, the sample value is greater than the mean of the blanks (defined at the mode of the posterior distribution), and the region of uncertainty surrounding the sample value fully excludes the 90% credible interval (C.I.) on the posterior distribution of the mean of the blanks. The grey shaded regions give the uncertainty range in the sample nuclide concentration. b, Nuclides are not credibly present above background: the sample value is less than or equal to the blank mean. c, Nuclides are not credibly present above background: although the sample value is greater than the blank mean, the region of uncertainty surrounding the sample value does not fully exclude the 90% C.I.
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Shakun, J.D., Corbett, L.B., Bierman, P.R. et al. Minimal East Antarctic Ice Sheet retreat onto land during the past eight million years. Nature 558, 284–287 (2018). https://doi.org/10.1038/s41586-018-0155-6
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