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Extensive retreat and re-advance of the West Antarctic Ice Sheet during the Holocene

Abstract

To predict the future contributions of the Antarctic ice sheets to sea-level rise, numerical models use reconstructions of past ice-sheet retreat after the Last Glacial Maximum to tune model parameters1. Reconstructions of the West Antarctic Ice Sheet have assumed that it retreated progressively throughout the Holocene epoch (the past 11,500 years or so)2,3,4. Here we show, however, that over this period the grounding line of the West Antarctic Ice Sheet (which marks the point at which it is no longer in contact with the ground and becomes a floating ice shelf) retreated several hundred kilometres inland of today’s grounding line, before isostatic rebound caused it to re-advance to its present position. Our evidence includes, first, radiocarbon dating of sediment cores recovered from beneath the ice streams of the Ross Sea sector, indicating widespread Holocene marine exposure; and second, ice-penetrating radar observations of englacial structure in the Weddell Sea sector, indicating ice-shelf grounding. We explore the implications of these findings with an ice-sheet model. Modelled re-advance of the grounding line in the Holocene requires ice-shelf grounding caused by isostatic rebound. Our findings overturn the assumption of progressive retreat of the grounding line during the Holocene in West Antarctica, and corroborate previous suggestions of ice-sheet re-advance5. Rebound-driven stabilizing processes were apparently able to halt and reverse climate-initiated ice loss. Whether these processes can reverse present-day ice loss6 on millennial timescales will depend on bedrock topography and mantle viscosity—parameters that are difficult to measure and to incorporate into ice-sheet models.

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Fig. 1: Basal topography and surface ice-flow speed in the Weddell and Ross Sea sectors of West Antarctica.
Fig. 2: Ice-penetrating radar evidence for grounding of the Ronne Ice Shelf.
Fig. 3: Modelled grounding-line retreat and re-advance due to lithospheric rebound.

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References

  1. DeConto, R. M. & Pollard, D. Contribution of Antarctica to past and future sea-level rise. Nature 531, 591–597 (2016).

    Article  ADS  PubMed  CAS  Google Scholar 

  2. Bentley, M. J. et al. A community-based geological reconstruction of Antarctic Ice Sheet deglaciation since the Last Glacial Maximum. Quat. Sci. Rev. 100, 1–9 (2014).

    Article  ADS  Google Scholar 

  3. Conway, H. et al. Past and future grounding-line retreat of the West Antarctic Ice Sheet. Science 286, 280–283 (1999).

    Article  PubMed  CAS  Google Scholar 

  4. Spector, P. et al. Rapid early-Holocene deglaciation in the Ross Sea, Antarctica. Geophys. Res. Lett. 44, 7817–7825 (2017).

    Article  ADS  Google Scholar 

  5. Bradley, S. L. et al. Low post-glacial rebound rates in the Weddell Sea due to Late Holocene ice-sheet readvance. Earth Planet. Sci. Lett. 413, 79–89 (2015).

    Article  ADS  CAS  Google Scholar 

  6. Scambos, T. A. et al. How much, how fast? A science review and outlook for research on the instability of Antarctica’s Thwaites Glacier in the 21st century. Global Planet. Change 153, 16–34 (2017).

    Article  ADS  Google Scholar 

  7. Goodwin, I. D. Did changes in Antarctic ice volume influence late Holocene sea-level lowering? Quat. Sci. Rev. 17, 319–332 (1998).

    Article  ADS  Google Scholar 

  8. Halberstadt, A. R. W., Simkins, L. M., Greenwood, S. L. & Anderson, J. B. Past ice-sheet behaviour: retreat scenarios and changing controls in the Ross Sea, Antarctica. Cryosphere 10, 1003–1020 (2006).

    Article  ADS  Google Scholar 

  9. Catania, G. A. et al. Evidence for floatation or near floatation in the mouth of Kamb Ice Stream, West Antarctica, prior to stagnation. J. Geophys. Res. Earth Surf. 111, F01005 (2006).

    Article  ADS  Google Scholar 

  10. Siegert, M. et al. Late Holocene ice-flow reconfiguration in the Weddell Sea sector of West Antarctica. Quat. Sci. Rev. 78, 98–107 (2013).

    Article  ADS  Google Scholar 

  11. Adhikari, S. et al. Future Antarctic bed topography and its implications for ice sheet dynamics. Solid Earth 5, 569–584 (2014).

    Article  ADS  Google Scholar 

  12. Gomez, N., Pollard, D. & Holland, D. Sea-level feedback lowers projections of future Antarctic Ice-Sheet mass loss. Nat. Commun. 6, 8798 (2015).

    Article  ADS  PubMed  PubMed Central  CAS  Google Scholar 

  13. Greischar, L. L. & Bentley, C. R. Isostatic equilibrium grounding line between the West Antarctic inland ice sheet and the Ross Ice Shelf. Nature 283, 651–654 (1980).

    Article  ADS  Google Scholar 

  14. Konrad, H. et al. Potential of the solid-Earth response for limiting long-term West Antarctic Ice Sheet retreat in a warming climate. Earth Planet. Sci. Lett. 432, 254–264 (2015).

    Article  ADS  CAS  Google Scholar 

  15. Matsuoka, K. et al. Antarctic ice rises and rumples: their properties and significance for ice-sheet dynamics and evolution. Earth Sci. Rev. 150, 724–745 (2015).

    Article  Google Scholar 

  16. Thomas, R. H. The creep of ice shelves: interpretation of observed behavior. J. Glaciol. 12, 55–70 (1973).

    Article  ADS  Google Scholar 

  17. Hanna, E. et al. Ice-sheet mass balance and climate change. Nature 498, 51–59 (2013).

    Article  ADS  PubMed  CAS  Google Scholar 

  18. Kamb, B. in The West Antarctic Ice Sheet: Behavior and Environment (eds Alley, R. B. & Bindschadler, R. A.) 157–199 (American Geophysical Union, Washington DC, 2001).

  19. Scherer, R. P. Quaternary and tertiary microfossils from beneath ice stream B: evidence for a dynamic West Antarctic ice sheet history. Palaeogeogr. Palaeoclimatol. Palaeoecol. 90, 395–412 (1991).

    Article  Google Scholar 

  20. Livingstone, S. et al. Potential subglacial lake locations and meltwater drainage pathways beneath the Antarctic and Greenland ice sheets. Cryosphere 7, 1721–1740 (2013).

    Article  ADS  Google Scholar 

  21. Price, S. F., Conway, H. & Waddington, E. D. Evidence for late Pleistocene thinning of Siple Dome, West Antarctica. J. Geophys. Res. Earth Surf. 112, F03021 (2007).

    ADS  Google Scholar 

  22. Catania, G., Hulbe, C. & Conway, H. Grounding-line basal melt rates determined using radar-derived internal stratigraphy. J. Glaciol. 56, 545–554 (2010).

    Article  ADS  Google Scholar 

  23. Winkelmann, R. et al. The Potsdam Parallel Ice Sheet Model (PISM-PIK)—part 1: model description. Cryosphere 5, 715–726 (2011).

    Article  ADS  Google Scholar 

  24. Pollard, D. et al. Large ensemble modeling of the last deglacial retreat of the West Antarctic Ice Sheet: comparison of simple and advanced statistical techniques. Geosci. Model Dev. 9, 1697–1723 (2016).

    Article  ADS  Google Scholar 

  25. Golledge, N. R. et al. Antarctic contribution to meltwater pulse 1A from reduced Southern Ocean overturning. Nat. Commun. 5, 5107 (2014).

    Article  PubMed  CAS  Google Scholar 

  26. Maris, M. N. A. et al. A model study of the effect of climate and sea-level change on the evolution of the Antarctic Ice Sheet from the Last Glacial Maximum to 2100. Clim. Dyn. 45, 837–851 (2015).

    Article  Google Scholar 

  27. Pollard, D., Gomez, N. & Deconto, R. M. Variations of the Antarctic ice sheet in a coupled ice sheet-Earth-sea level model: sensitivity to viscoelastic Earth properties. J. Geophys. Res. Earth Surf. 122, 2124–2138 (2017).

    Article  ADS  Google Scholar 

  28. Graham, A. G. et al. Seabed corrugations beneath an Antarctic ice shelf revealed by autonomous underwater vehicle survey: origin and implications for the history of Pine Island Glacier. J. Geophys. Res. Earth Surf. 118, 1356–1366 (2013).

    Article  ADS  Google Scholar 

  29. Fretwell, P. et al. Bedmap2: improved ice bed, surface and thickness datasets for Antarctica. Cryosphere 7, 375–393 (2013).

    Article  ADS  Google Scholar 

  30. Rignot, E., Mouginot, J. & Scheuchl, B. Ice flow of the Antarctic ice sheet. Science 333, 1427–1430 (2011).

    Article  ADS  PubMed  CAS  Google Scholar 

  31. Depoorter, M. A. et al. Calving fluxes and basal melt rates of Antarctic ice shelves. Nature 502, 89–92 (2013).

    Article  ADS  PubMed  CAS  Google Scholar 

  32. Haran, T. et al. MODIS mosaic of Antarctica 2003–2004 (MOA2004) image map. US Antarctic Program Data Center https://doi.org/10.7265/N5ZK5DM5 (2005).

  33. Lipps, J. H., Ronan, T. DeLaca, T. Life below the Ross ice shelf. Antarct. Sci. 203, 447–449 (1979).

    CAS  Google Scholar 

  34. Coenen, J. J. Inferring West Antarctic Subglacial Basin History and Ice Stream Processes Using Siliceous Microfossils. MSc Thesis, Northern Illinois Univ. (2016).

  35. Scherer, R. P. et al. Pleistocene collapse of the West Antarctic ice sheet. Science 281, 82–85 (1998).

    Article  ADS  PubMed  CAS  Google Scholar 

  36. Abbott, M. B. & Stafford, T. W. Jr. Radiocarbon geochemistry of modern and ancient Arctic lake systems, Baffin Island, Canada. Quat. Res. 45, 300–311 (1996).

    Article  CAS  Google Scholar 

  37. Priscu, J. C. et al. A microbiologically clean strategy for access to the Whillans Ice Stream subglacial environment. Antarct. Sci. 25, 637–647 (2013).

    Article  ADS  Google Scholar 

  38. Rosenheim, B. E. et al. Improving Antarctic sediment 14 C dating using ramped pyrolysis: an example from the Hugo Island trough. Radiocarbon 55, 115–126 (2013).

    Article  CAS  Google Scholar 

  39. Clark, P. U. et al. The last glacial maximum. Science 325, 710–714 (2009).

    Article  ADS  PubMed  CAS  Google Scholar 

  40. Anderson, J. B. et al. Ross Sea paleo-ice sheet drainage and deglacial history during and since the LGM. Quat. Sci. Rev. 100, 31–54 (2014).

    Article  ADS  Google Scholar 

  41. Andrews, J. T. et al. Problems and possible solutions concerning radiocarbon dating of surface marine sediments, Ross Sea, Antarctica. Quat. Res. 52, 206–216 (1999).

    Article  CAS  Google Scholar 

  42. Licht, K. J. & Andrews, J. T. The 14C record of Late Pleistocene ice advance and retreat in the central Ross Sea, Antarctica. Arct. Antarct. Alp. Res. 34, 324–333 (2002).

    Article  Google Scholar 

  43. McKay, R. et al. Retreat history of the Ross Ice Sheet (Shelf) since the Last Glacial Maximum from deep-basin sediment cores around Ross Island. Palaeogeogr. Palaeoclimatol. Palaeoecol. 260, 245–261 (2008).

    Article  Google Scholar 

  44. Martinerie, P. et al. Physical and climatic parameters which influence the air content in polar ice. Earth Planet. Sci. Lett. 112, 1–13 (1992).

    Article  ADS  Google Scholar 

  45. Federer, U. et al. Continuous flow analysis of total organic carbon in polar ice cores. Environ. Sci. Technol. 42, 8039–8043 (2008).

    Article  ADS  PubMed  CAS  Google Scholar 

  46. Antony, R. et al. Organic carbon in Antarctic snow: spatial trends and possible sources. Environ. Sci. Technol. 45, 9944–9950 (2011).

    Article  ADS  PubMed  CAS  Google Scholar 

  47. Joughin, I. et al. Melting and freezing beneath the Ross ice streams, Antarctica. J. Glaciol. 50, 96–108 (2004).

    Article  ADS  Google Scholar 

  48. Christner, B. C. et al. A microbial ecosystem beneath the West Antarctic ice sheet. Nature 512, 310–313 (2014).

    Article  PubMed  CAS  Google Scholar 

  49. Tulaczyk, S., Kamb, B. & Engelhardt, H. F. Estimates of effective stress beneath a modern West Antarctic ice stream from till preconsolidation and void ratio. Boreas 30, 101–114 (2001).

    Article  Google Scholar 

  50. Christianson, K. et al. Basal conditions at the grounding zone of Whillans Ice Stream, West Antarctica, from ice-penetrating radar. J. Geophys. Res. Earth Surf. 121, 1954–1983 (2016).

    Article  ADS  Google Scholar 

  51. Hall, B. L. et al. Constant Holocene Southern-Ocean 14 C reservoir ages and ice-shelf flow rates. Earth Planet. Sci. Lett. 296, 115–123 (2010).

    Article  ADS  CAS  Google Scholar 

  52. Van Liefferinge, B. & Pattyn, F. Using ice-flow models to evaluate potential sites of million year-old ice in Antarctica. Clim. Past 9, 2335 (2013).

    Article  Google Scholar 

  53. Kingslake, J. et al. Ice-flow reorganization in West Antarctica 2.5 kyr ago dated using radar-derived englacial flow velocities. Geophys. Res. Lett. 43, 9103–9112 (2016).

    Article  ADS  Google Scholar 

  54. Scambos, T., Haran, T., Fahnestock, M., Painter, T. & Bohlander, J. MODIS-based Mosaic of Antarctica (MOA) data sets: continent-wide surface morphology and snow grain size. Remote Sens. Environ. 111, 242–257 (2007).

    Article  ADS  Google Scholar 

  55. Ely, J. et al. Insights on the formation of longitudinal surface structures on ice sheets from analysis of their spacing, spatial distribution, and relationship to ice thickness and flow. J. Geophys. Res. Earth Surf. 122, 961–972 (2017).

    Article  ADS  Google Scholar 

  56. Favier, L. & Pattyn, F. Antarctic ice rise formation, evolution, and stability. Geophys. Res. Lett. 42, 4456–4463 (2015).

    Article  ADS  Google Scholar 

  57. Bindschadler, R. A., Roberts, E. P. & Iken, A. Age of Crary Ice Rise, Antarctica, determined from temperature-depth profiles. Ann. Glaciol. 14, 13–16 (1990).

    Article  ADS  Google Scholar 

  58. Bueler, E. & Brown, J. Shallow shelf approximation as a “sliding law” in a thermomechanically coupled ice sheet model. J. Geophys. Res. Earth Surf. 114, F03008 (2009).

    Article  ADS  Google Scholar 

  59. The PISM authors. PISM, a Parallel Ice Sheet Model: user’s manual (2017), based on development revision e9d2d1f8 (7 March 2017), http://www.pism-docs.org/wiki/lib/exe/fetch.php?media=pism_manual.pdf (2017).

  60. Cuffey, K. M. et al. Deglacial temperature history of West Antarctica. Proc. Natl Acad. Sci. USA 113, 14249–14254 (2016).

    Article  ADS  PubMed  PubMed Central  CAS  Google Scholar 

  61. Ligtenberg, S. et al. Future surface mass balance of the Antarctic ice sheet and its influence on sea level change, simulated by a regional atmospheric climate model. Clim. Dyn. 41, 867–884 (2013).

    Article  Google Scholar 

  62. Frieler, K. et al. Consistent evidence of increasing Antarctic accumulation with warming. Nat. Clim. Chang. 5, 348–352 (2015).

    Article  ADS  Google Scholar 

  63. Reese, R. et al. Antarctic sub-shelf melt rates via PICO. Cryosphere Discuss. https://doi.org/10.5194/tc-2017-70 (2017).

  64. Schmidtko, S. et al. Multidecadal warming of Antarctic waters. Science 346, 1227–1231 (2014).

    Article  ADS  PubMed  CAS  Google Scholar 

  65. Li, C., von Storch, J. S. & Marotzke, J. Deep-ocean heat uptake and equilibrium climate response. Clim. Dyn. 40, 1071–1086 (2013).

    Article  Google Scholar 

  66. Levermann, A. et al. Kinematic first-order calving law implies potential for abrupt ice-shelf retreat. Cryosphere 6, 273–286 (2012).

    Article  ADS  Google Scholar 

  67. Pollard, D. & DeConto, R. A. simple inverse method for the distribution of basal sliding coefficients under ice sheets, applied to Antarctica. Cryosphere 6, 953 (2012).

    Article  ADS  Google Scholar 

  68. Feldmann, J. et al. Resolution-dependent performance of grounding line motion in a shallow model compared with a full-Stokes model according to the MISMIP3d intercomparison. J. Glaciol. 60, 353–360 (2014).

    Article  ADS  Google Scholar 

  69. Stuhne, G. & Peltier, W. Reconciling the ICE-6G_C reconstruction of glacial chronology with ice sheet dynamics: the cases of Greenland and Antarctica. J. Geophys. Res. Earth Surf. 120, 1841–1865 (2015).

    Article  ADS  Google Scholar 

  70. Bueler, E., Lingle, C. S. & Brown, J. Fast computation of a viscoelastic deformable Earth model for ice-sheet simulations. Ann. Glaciol. 46, 97–105 (2007).

    Article  ADS  Google Scholar 

  71. Milne, G., Mitrovica, J. X. & Davis, J. L. Near-field hydro-isostasy: the implementation of a revised sea-level equation. Geophys. J. Int. 139, 464–482 (1999).

    Article  ADS  Google Scholar 

  72. Pritchard, H. D. Bedgap: where next for Antarctic subglacial mapping? Antarct. Sci. 26, 742–757 (2014).

    Article  ADS  Google Scholar 

  73. Jones, P. W. First- and second-order conservative remapping schemes for grids in spherical coordinates. Mon. Weath. Rev. 127, 2204–2210 (1999).

    Article  ADS  Google Scholar 

  74. Pollard, D. & DeConto, R. M. Description of a hybrid ice sheet-shelf model, and application to Antarctica. Geosci. Model Dev. 5, 1273–1295 (2012).

    Article  ADS  Google Scholar 

  75. Briggs, R. D., Pollard, D. & Tarasov, L. A data-constrained large ensemble analysis of Antarctic evolution since the Eemian. Quat. Sci. Rev. 103, 91–115 (2014).

    Article  ADS  Google Scholar 

  76. Pollard, D., Chang, W., Haran, M., Applegate, P. & DeConto, R. Large ensemble modeling of the last deglacial retreat of the West Antarctic Ice Sheet: comparison of simple and advanced statistical techniques. Geosci. Mod. Dev. 9, 1697–1723 (2016).

    Article  Google Scholar 

  77. Bindschadler, R. A. et al. Ice-sheet model sensitivities to environmental forcing and their use in projecting future sea level (the SeaRISE project). J. Glaciol. 59, 195–224 (2013).

    Article  ADS  Google Scholar 

  78. Lambeck, K. et al. Sea level and global ice volumes from the Last Glacial Maximum to the Holocene. Proc. Natl Acad. Sci. USA 111, 15296–15303 (2014).

    Article  ADS  PubMed  PubMed Central  CAS  Google Scholar 

  79. Bintanja, R. & Van de Wal, R. North American ice-sheet dynamics and the onset of 100,000-year glacial cycles. Nature 454, 869–872 (2008).

    Article  ADS  PubMed  CAS  Google Scholar 

  80. Imbrie, J. D. & McIntyre, A. SPECMAP time scale developed by Imbrie et al., 1984 based on normalized planktonic records (normalized O-18 vs time, specmap.017). Pangaea https://doi.org/10.1594/PANGAEA.441706 (2006).

  81. Gomez, N., Pollard, D. & Mitrovica, J. X. A 3-D coupled ice sheet–sea level model applied to Antarctica through the last 40 ky. Earth Planet. Sci. Lett. 384, 88–99 (2013).

    Article  ADS  CAS  Google Scholar 

  82. Whitehouse, P. L., Bentley, M. J., Milne, G. A., King, M. A. & Thomas, I. D. A new glacial isostatic model for Antarctica: calibrated and tested using observations of relative sea-level change and present-day uplift rates. Geophys. J. Int. 190, 1464–1482 (2012).

    Article  ADS  Google Scholar 

  83. Jouzel, J. et al. Orbital and millennial Antarctic climate variability over the past 800,000 years. Science 317, 793–796 (2007).

    Article  ADS  PubMed  CAS  Google Scholar 

  84. Fudge, T. et al. Variable relationship between accumulation and temperature in West Antarctica for the past 31,000 years. Geophys. Res. Lett. 43, 3795–3803 (2016).

    Article  ADS  Google Scholar 

  85. Hay, C. C. et al. Sea level fingerprints in a region of complex Earth structure: the case of WAIS. J. Clim. 30, 1881–1892 (2017).

    Article  ADS  Google Scholar 

  86. Ji, F. et al. Variations of the effective elastic thickness over the Ross Sea and Transantarctic Mountains and implications for their structure and tectonics. Tectonophysics 717, 127–138 (2017).

    Article  ADS  Google Scholar 

  87. Chen, B., Haeger, C., Kaban, M. K. & Petrunin, A. G. Variations of the effective elastic thickness reveal tectonic fragmentation of the Antarctic lithosphere. Tectonophysics https://doi.org/10.1016/j.tecto.2017.06.012 (2017).

  88. Hein, A. S. et al. Mid-Holocene pulse of thinning in the Weddell Sea sector of the West Antarctic ice sheet. Nat. Commun. 7, 12511 (2016).

    Article  ADS  PubMed  PubMed Central  CAS  Google Scholar 

  89. Balco, G. et al. Cosmogenic-nuclide exposure ages from the Pensacola Mountains adjacent to the Foundation Ice Stream, Antarctica. Am. J. Sci. 316, 542–577 (2016).

    Article  ADS  CAS  Google Scholar 

  90. Bentley, M. J. et al. Deglacial history of the Pensacola Mountains, Antarctica from glacial geomorphology and cosmogenic nuclide surface exposure dating. Quat. Sci. Rev. 158, 58–76 (2017).

    Article  ADS  Google Scholar 

  91. Whitehouse, P. L. et al. Controls on Last Glacial Maximum ice extent in the Weddell Sea embayment, Antarctica. J. Geophys. Res. Earth Surf. 122, 371–397 (2017).

    Article  ADS  Google Scholar 

  92. Ross, N. et al. Steep reverse bed slope at the grounding line of the Weddell Sea sector in West Antarctica. Nat. Geosci. 5, 393 (2012).

    Article  ADS  CAS  Google Scholar 

  93. Todd, C., Stone, J., Conway, H., Hall, B. & Bromley, G. Late Quaternary evolution of Reedy Glacier, Antarctica. Quat. Sci. Rev. 29, 1328–1341 (2010).

    Article  ADS  Google Scholar 

  94. Jezek, K. C., Curlander, J. C., Carsey, F., Wales, C & Barry, R. RAMP AMM-1 SAR image mosaic of Antarctica, version 2. National Snow and Ice Data Center https://doi.org/10.5067/8AF4ZRPULS4H (2013).

  95. Fürst, J. J. et al. The safety band of Antarctic ice shelves. Nat. Clim. Chang. 6, 479–482 (2016).

    Article  Google Scholar 

  96. WAIS Divide Project Members. Precise interpolar phasing of abrupt climate change during the last ice age. Nature 520, 661–665 (2015).

    Article  ADS  CAS  Google Scholar 

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Acknowledgements

J.K. and the Weddell Sea fieldwork were funded by Natural Environmental Research Council (NERC) grant NE/J008087/1, led by R. Hindmarsh. Logistical support was provided by many members of the British Antarctic Survey’s air unit and field operations team. We particularly thank I. Rudkin and S. Webster for assistance in the field. We also thank H. Pritchard for supplying bed elevation data and Schlumberger Limited for a software donation. PISM development is supported by NASA grants NNX13AM16G and NNX13AK27G. T.A. is supported by the Deutsche Forschungsgemeinschaft (DFG) in the framework of the priority program ‘Antarctic Research with comparative investigations in Arctic ice areas’ through grants LE1448/6-1 and LE1448/7-1.We acknowledge the European Regional Development Fund, the German Federal Ministry of Education and Research, and the Land Brandenburg for providing high-performance computer resources at the Potsdam Institute for Climate Impact Research. We also thank the Gauss Centre for Supercomputing e.V. (http://www.gauss-centre.eu) for providing computing time on the GCS Supercomputer SuperMUC at Leibniz Supercomputing Centre (http://www.lrz.de; project code pr94ga). We thank C. Buizert for providing ice-core temperature reconstructions; D. Peltier for access to eustatic sea-level reconstructions; J. Lenaerts for surface mass balance data from the RACMO climate model; and S. Jamieson for providing the RAISED consortium’s grounding-line reconstructions. R.P.S., J.C., R.D.P. and S.T. were funded by National Science Foundation (NSF) WISSARD Project grants ANT-0839107, ANT-0839142, ANT-0838947 and ANT-0839059. Collection of subglacial sediment samples at Subglacial Lake Whillans and the Whillans Grounding Zone was facilitated by the US Antarctic Program and the efforts of multiple field support teams, including the drilling team from the University of Nebraska–Lincoln and WISSARD traverse personnel, as well as by Air National Guard and Kenn Borek Air who provided air support. WIS, KIS and BIS samples were recovered by B. Kamb’s program at the California Institute of Technology (1988–2001), which included R.P.S. and S.T.; samples from the US Antarctic Program’s Ross Ice Shelf Project (1977–1979) cores were made available for study by the US Antarctic Sediment Core Repository, Florida State University. P.L.W. is funded by a NERC Independent Research Fellowship (NE/K009958/1). This research is a contribution to the Scientific Committee on Antarctic Research (SCAR) Solid Earth Response and Influence on Cryosphere Evolution (SERCE) program. We thank R. Arthern, R. Bell, R. Hindmarsh, C. Martín, J. Southon and K. Tinto for discussions that contributed to this study. We particularly thank D. Pollard for sharing ideas and unpublished Penn State model outputs for discussion.

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Nature thanks R. Drews, J. Smith and the other anonymous reviewer(s) for their contribution to the peer review of this work.

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Authors and Affiliations

Authors

Contributions

All authors contributed to manuscript preparation. T.A., J.K. and R.P.S. are co-lead authors with equal contributions; others are listed alphabetically. J.K. designed and conducted the Weddell Sea sector ice-penetrating radar survey and led the preparation of the manuscript. R.P.S., J.C., R.D.P. and S.T. collected and analysed sub-ice sediment samples as part of the WISSARD and earlier drilling projects in the Ross Sea sector. N.D.S. and J.C. prepared samples and interpreted 14C and 13C results. T.A. ran the PISM simulations and an extended analysis of parameter sensitivity. R.R. designed and analysed experiments for disentangling drivers of re-advance. M.G.W. analysed radar data from the Weddell Sea sector. P.L.W. provided input on parameterization of solid-Earth rebound and sea-level forcing for the model experiments.

Corresponding author

Correspondence to J. Kingslake.

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Extended data figures and tables

Extended Data Fig. 1 Relic crevasses in Henry Ice Rise.

a, Radargram, aligned perpendicular to the divide ridge (inset shows the location). One undulating isochrone is delineated with colours showing normalized elevation. b, c, Close-up views of the boxed regions indicated in a. In both close-up panels, diffractors (hyperbolic reflectors) are interpreted as expressions of relic crevasses (data are unmigrated). The red vertical dashed line is the present-day grounding line31. df, Radargrams aligned approximately perpendicular to northern relic crevasses (d and e show migrated data). In c (6 km ≤ x ≤ 8 km) and f (0.3 km ≤ x ≤ 1.4 km) isochrones intercepting the bed are evident. g, Three relic crevasses mapped across several radar lines over a Radarsat Antarctic Mapping Project (RAMP) image94. The inset is an oblique, three-dimensional view of the features over an interpolated surface, showing the bed elevation zb (see Methods). Crevasse spacing in these areas ranges between approximately 200 m and 600 m. The arrow indicates the view direction of the oblique view.

Extended Data Fig. 2 Crevassing at Doake Ice Rumples.

a, RAMP94 image showing the surface expression of ice-shelf crevasses in synthetic aperture radar data. Light areas indicate high backscatter from (near-)surface reflectors, interpreted to be surface crevasses. Crevasses form over and immediately downstream of Doake Ice Rumples. We hypothesize that crevasses once formed in a similar manner over the topographic high beneath the northern tip of HIR. b, Close-up view of the crevasses (the black box in a shows the location), whose spacing (100–300 m), orientation (perpendicular to the flow of the ice shelf) and lateral extent (roughly 10 km) are similar to the steeply dipping reflectors discovered near the bed of the northern tip of HIR (for example, Extended Data Fig. 2g) in the region of a topographic high. Yellow curves are flow lines computed from satellite-derived surface velocities30. Flow is from bottom to top. Polar stereographic coordinates are in km. The present-day grounding line31 is in red.

Extended Data Fig. 3 Modelled grounding-line retreat and lithospheric rebound.

Cross-sections along transects through the Weddell (left) and Ross (right) Sea sectors, at 5-kyr intervals (for transect locations, see Fig. 3). The horizontal axis shows the distance from the present-day grounding line. The vertical blue dashed line shows the position of maximum grounding-line retreat. a, b, 15 kyr bp, with the grounding line close to the continental shelf edge. c, d, 10 kyr bp, with the grounding line having retreated to approximately its minimum, most retreated location. e, f, 5 kyr bp, with both ice shelves grounded on sub-ice-shelf bathymetric highs owing to seafloor uplift. g, h, Present day, with the grounding line having re-advanced to roughly the present-day configuration in response to the grounding of the ice shelf and uplift at the grounding line. The Crary, Bungenstock and Henry ice rises (CIR, BIR and HIR) are labelled in g and h. The Whillans Ice Stream (WIS) and Subglacial Lake Whillans (SLW) sediment-core locations are labelled in d. Blue dotted lines show the observed present-day ice-sheet bed, ocean floor and ice surface29, remapped on to the 15-km grid of the ice-sheet model.

Extended Data Fig. 4 Drivers of re-advance and the impact of bed re-mapping.

a, b, Results from four simulations (the reference simulation, and three additional experiments) designed to examine the cause of re-advance in the Weddell Sea (a) and Ross Sea (b) sectors (Methods). The most inland grounding-line location in the reference simulation, at around 10 kyr bp, is in blue. The colour map shows the flow buttressing number95 at 10 kyr bp in the ‘No uplift, grounding of ice rises’ experiment. The ice-front position is in grey. Background images over the grounded ice sheet are from MOA32. c, Basal topography and bathymetry in the Weddell Sea sector (with the grounding line in red) according to a 1-km-resolution dataset, constrained by geophysical observations (Bedmap 2; ref. 29). d, Conservative remapping of these data to 15-km resolution. Remapping substantially lowers the apparent maximum bed elevations beneath ice rises in the Weddell Sea sector: 135 m at KIR, 112 m at HIR and 36 m at BIR.

Extended Data Fig. 5 True and apparent ages of radiocarbon.

The 11 grey lines show exponential 14C-decay curves connecting the 14C/12C ratios (scale on the left) measured on acid-insoluble inorganics (AIOs) from our subglacial sediment samples to the apparent radiocarbon ages calculated from these measurements. The latter calculation assumes that the initial 14C/12C ratios in AIOs were equal to the modern ratio in radiocarbon dating standards. As discussed in the text and Methods, organic matter in Antarctic glacigenic sediments frequently contains an admixture of old 14C-dead material41,42. The record of oxygen isotopes in water ice from the WAIS Divide ice core (green line, with scale on the right) provides climatic context for the period between now and 35 kyr bp (ref. 96). Three key climatic periods are labelled: WAIS LGM39, Antarctic cold reversal (ACR) and Holocene.

Extended Data Fig. 6 Model sensitivity to forcings.

In the middle and right panels are time series of grounding-line position along transects, showing model sensitivity in the Weddell Sea (middle panels) and Ross Sea (right panels) sectors to: a, different sea-level reconstructions69,78,79,80; b, different scalings of the sea-level forcing to mimic self-gravitational effects; c, different surface-temperature forcings; and d, different accumulation forcings. In the left panels are: a, four alternative sea-level reconstructions; b, three alternative scalings of the reference-simulation sea-level forcing and a version that has been uniformly shifted 2,000 years earlier; c, temperature reconstructions from two ice cores, WAIS Divide and EPICA Dome C (EDC), and a reconstruction from the Last Interglacial (from EDC data); and d, four alternative accumulation histories. The constant LGM accumulation uses the EPICA Dome C core83 and a scaling of 2% per degree. Temperature and accumulation are expressed relative to the present day. Grounding-line positions are relative to the present-day position (vertical dashed line) along the transacts shown in Fig. 3. In all simulations, the grounding line is in its most advanced position, up to 1,000 km beyond its present-day position, before MWP1a (14.4 kyr bp; horizontal dotted line). During the Holocene the grounding line retreats up to 500 km upstream of its present location, and usually re-advances towards its present-day position. Grey shading indicates the spread of grounding-line responses, and grey curves show the mean of each sensitivity experiment. In each case the violet curve shows the reference simulation. Grounding-line positions (based on marine and terrestrial geological evidence) from the RAISED reconstruction with associated uncertainties are shown in black2.

Extended Data Fig. 7 Model sensitivity to parameters.

Time series of grounding-line position along transects, showing model sensitivity in the Weddell and Ross Sea sectors to: a, mantle viscosity, μ, and the flexural rigidity of the lithosphere, D; b, c, enhancement factors ESSA and ESIA; d, the sliding-law exponent, q; e, the till water decay rate, T, and till effective pressure fraction, N; f, minimum till friction angle and the method used to derive the friction angle (see Methods); g PICO ocean model parameters for overturning strength, C, and heat exchange, g; and h, the dependence of calving rate on the ice-shelf spreading rate, K (Extended Data Table 2). In each panel, the violet curve shows the reference simulation. Grounding-line positions (based on marine and terrestrial geological evidence) from the RAISED reconstruction, with associated uncertainties, are shown in black2.

Extended Data Fig. 8 Model sensitivity to spatial resolution.

The results of three simulations using different grid resolutions: a, 15 km (reference simulation; identical to Fig. 3); b, 10 km; and c, 7 km. Owing to computational limitations, the two higher-resolution simulations cover only the past 20 kyr, so they lack a higher-resolution spin-up period. These higher-resolution simulations display similar Holocene retreat and re-advance driven by isostatic rebound to the reference simulation, but the LGM extent and grounding-line re-advance in the Weddell Sea are much less. A full exploration of the resolution dependence of the model requires using higher resolution during entire simulations for all ensemble members. This is limited at present by computing resources. Background shading shows basal topography and bathymetry29.

Extended Data Table 1 Results of radiocarbon and δ13C analyses of subglacial sediments
Extended Data Table 2 Key model parameters, with modelled retreat and re-advance

Supplementary information

Supplementary Video 1: Reference numerical ice-sheet model simulation of WAIS for the past 35 kyr

Top-left panel shows the vertically averaged ice speed (logarithmic colour scale). Lower-left panel shows the bedrock rebound rate. Notice the rapid rebound following deglaciation in the Weddell and Ross Sea sectors. Upper-right panel shows modelled surface elevation relative to present day on grounded ice and basal melt rates beneath ice shelves. Lower-right panel shows time series of the sea-level forcing (left vertical axis), the temperature forcing (right vertical axis) and the above-flotation volume of the ice sheet expressed in sea-level equivalent, assuming a constant ocean area of 3.61×1014 m2. See Methods for details of forcings and parameterisations.

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Kingslake, J., Scherer, R.P., Albrecht, T. et al. Extensive retreat and re-advance of the West Antarctic Ice Sheet during the Holocene. Nature 558, 430–434 (2018). https://doi.org/10.1038/s41586-018-0208-x

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