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The multi-millennial Antarctic commitment to future sea-level rise

Abstract

Atmospheric warming is projected to increase global mean surface temperatures by 0.3 to 4.8 degrees Celsius above pre-industrial values by the end of this century1. If anthropogenic emissions continue unchecked, the warming increase may reach 8–10 degrees Celsius by 2300 (ref. 2). The contribution that large ice sheets will make to sea-level rise under such warming scenarios is difficult to quantify because the equilibrium-response timescale of ice sheets is longer than those of the atmosphere or ocean. Here we use a coupled ice-sheet/ice-shelf model to show that if atmospheric warming exceeds 1.5 to 2 degrees Celsius above present, collapse of the major Antarctic ice shelves triggers a centennial- to millennial-scale response of the Antarctic ice sheet in which enhanced viscous flow produces a long-term commitment (an unstoppable contribution) to sea-level rise. Our simulations represent the response of the present-day Antarctic ice-sheet system to the oceanic and climatic changes of four representative concentration pathways (RCPs) from the Fifth Assessment Report of the Intergovernmental Panel on Climate Change3. We find that substantial Antarctic ice loss can be prevented only by limiting greenhouse gas emissions to RCP 2.6 levels. Higher-emissions scenarios lead to ice loss from Antarctic that will raise sea level by 0.6–3 metres by the year 2300. Our results imply that greenhouse gas emissions in the next few decades will strongly influence the long-term contribution of the Antarctic ice sheet to global sea level.

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Figure 1: Modelled ice-sheet evolution under Antarctic-specific RCP-based warming scenarios.
Figure 2: Antarctic Ice Sheet (AIS) contribution to GMSL.
Figure 3: Response of modelled Antarctic ice sheet to simplified environmental forcings.
Figure 4: Glaciological changes taking place under single-parameter environmental perturbations.

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References

  1. Meinshausen, M. et al. The RCP greenhouse gas concentrations and their extensions from 1765 to 2300. Clim. Change 109, 213–241 (2011)

    Article  ADS  CAS  Google Scholar 

  2. Rogelj, J., Meinshausen, M. & Knutti, R. Global warming under old and new scenarios using IPCC climate sensitivity range estimates. Nature Clim. Change 2, 248–253 (2012)

    Article  ADS  Google Scholar 

  3. Collins, M. et al. in Climate Change 2013: The Physical Science Basis. Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change (eds Stocker, T. et al.) 1029–1136 (Cambridge Univ. Press, 2013)

    Google Scholar 

  4. Pritchard, H. D. et al. Antarctic ice-sheet loss driven by basal melting of ice shelves. Nature 484, 502–505 (2012)

    Article  ADS  CAS  Google Scholar 

  5. Wouters, B. et al. Dynamic thinning of glaciers on the Southern Antarctic Peninsula. Science 348, 899–903 (2015)

    Article  ADS  CAS  Google Scholar 

  6. Joughin, I. & Alley, R. B. Stability of the West Antarctic ice sheet in a warming world. Nature Geosci. 4, 506–513 (2011)

    Article  ADS  CAS  Google Scholar 

  7. Scambos, T. A., Bohlander, J. A., Shuman, C. A. & Skvarca, P. Glacier acceleration and thinning after ice shelf collapse in the Larsen B embayment, Antarctica. Geophys. Res. Lett. 31, L18402 (2004)

    Article  ADS  Google Scholar 

  8. Vaughan, D. G. & Doake, C. S. M. Recent atmospheric warming and retreat of ice shelves on the Antarctic Peninsula. Nature 379, 328–331 (1996)

    Article  ADS  CAS  Google Scholar 

  9. Liu, Y. et al. Ocean-driven thinning enhances iceberg calving and retreat of Antarctic ice shelves. Proc. Natl Acad. Sci. USA 112, 3263–3268 (2015)

    Article  ADS  CAS  Google Scholar 

  10. Paolo, F. S., Fricker, H. A. & Padman, L. Volume loss from Antarctic ice shelves is accelerating. Science 348, 327–331 (2015)

    Article  ADS  CAS  Google Scholar 

  11. Roemmich, D. et al. Unabated planetary warming and its ocean structure since 2006. Nature Clim. Change 5, 240–245 (2015)

    Article  ADS  Google Scholar 

  12. Schmidtko, S., Heywood, K. J., Thompson, A. F. & Aoki, S. Multidecadal warming of Antarctic waters. Science 346, 1227–1231 (2014)

    Article  ADS  CAS  Google Scholar 

  13. Steig, E. J. et al. Warming of the Antarctic ice-sheet surface since the 1957 International Geophysical Year. Nature 457, 459–462 (2009)

    Article  ADS  CAS  Google Scholar 

  14. Harig, C. & Simons, F. J. Accelerated West Antarctic ice mass loss continues to outpace East Antarctic gains. Earth Planet. Sci. Lett. 415, 134–141 (2015)

    Article  ADS  CAS  Google Scholar 

  15. Hay, C. C., Morrow, E., Kopp, R. E. & Mitrovica, J. X. Probabilistic reanalysis of twentieth-century sea-level rise. Nature 517, 481–484 (2015)

    Article  ADS  CAS  Google Scholar 

  16. Joughin, I., Smith, B. E. & Medley, B. Marine ice sheet collapse potentially under way for the Thwaites Glacier basin, West Antarctica. Science 344, 735–738 (2014)

    Article  ADS  CAS  Google Scholar 

  17. Rignot, E., Mouginot, J., Morlighem, M., Seroussi, H. & Scheuchl, B. Widespread, rapid grounding line retreat of Pine Island, Thwaites, Smith, and Kohler glaciers, West Antarctica, from 1992 to 2011. Geophys. Res. Lett. 41, 3502–3509 (2014)

    Article  ADS  Google Scholar 

  18. Bindschadler, R. 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 

  19. Levermann, A. et al. Projecting Antarctic ice discharge using response functions from SeaRISE ice-sheet models. Earth Syst. Dyn. 5, 271–293 (2014)

    Article  ADS  Google Scholar 

  20. Levermann, A. et al. The multimillennial sea-level commitment of global warming. Proc. Natl Acad. Sci. USA 110, 13745–13750 (2013)

    Article  ADS  CAS  Google Scholar 

  21. Naish, T. et al. Obliquity-paced Pliocene West Antarctic ice sheet oscillations. Nature 458, 322–328 (2009)

    Article  ADS  CAS  Google Scholar 

  22. Pollard, D. & DeConto, R. M. Modelling West Antarctic ice sheet growth and collapse through the past five million years. Nature 458, 329–332 (2009)

    Article  ADS  CAS  Google Scholar 

  23. Schaeffer, M., Hare, W., Rahmstorf, S. & Vermeer, M. Long-term sea-level rise implied by 1.5 °C and 2 °C warming levels. Nature Clim. Change 2, 867–870 (2012)

    Article  ADS  Google Scholar 

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

    Article  ADS  Google Scholar 

  25. Winkelmann, R. et al. The Potsdam Parallel Ice Sheet Model (PISM-PIK)—Part 1: Model description. Cryosphere 5, 715–726 (2010)

    Article  ADS  Google Scholar 

  26. Feldmann, J. & Levermann, A. Interaction of marine ice-sheet instabilities in two drainage basins: simple scaling of geometry and transition time. Cryosphere 9, 631–645 (2015)

    Article  ADS  Google Scholar 

  27. Feldmann, J., Albrecht, T., Khroulev, C., Pattyn, F. & Levermann, A. Resolution-dependent performance of grounding line motion in a shallow model compared to a full-Stokes model according to the MISMIP3d intercomparison. J. Glaciol. 60, 353–360 (2014)

    Article  ADS  Google Scholar 

  28. Clarke, G. K., Nitsan, U. & Paterson, W. Strain heating and creep instability in glaciers and ice sheets. Rev. Geophys. 15, 235–247 (1977)

    Article  ADS  Google Scholar 

  29. Winkelmann, R., Levermann, A., Frieler, K. & Martin, M. Increased future ice discharge from Antarctica owing to higher snowfall. Nature 492, 239–242 (2012)

    Article  ADS  CAS  Google Scholar 

  30. Meinshausen, M. et al. Greenhouse-gas emission targets for limiting global warming to 2 °C. Nature 458, 1158–1162 (2009)

    Article  ADS  CAS  Google Scholar 

  31. Favier, L. et al. Retreat of Pine Island Glacier controlled by marine ice-sheet instability. Nature Clim. Change 4, 117–121 (2014)

    Article  ADS  Google Scholar 

  32. Cornford, S. et al. Century-scale simulations of the response of the West Antarctic Ice Sheet to a warming climate. Cryosphere 9, 1579–1600 (2015)

    Article  ADS  Google Scholar 

  33. Schoof, C. A variational approach to ice stream flow. J. Fluid Mech. 556, 227–251 (2006)

    Article  ADS  MathSciNet  Google Scholar 

  34. Leguy, G. R., Asay-Davis, X. S. & Lipscomb, W. H. Parameterization of basal friction near grounding lines in a one-dimensional ice sheet model. Cryosphere 8, 1239–1259 (2014)

    Article  ADS  Google Scholar 

  35. Tsai, V. C., Stewart, A. L. & Thompson, A. F. Marine ice-sheet profiles and stability under Coulomb basal conditions. J. Glaciol. 61, 205–215 (2015)

    Article  ADS  Google Scholar 

  36. Holland, D. M. & Jenkins, A. Modeling thermodynamic ice-ocean interactions at the base of an ice shelf. J. Phys. Oceanogr. 29, 1787–1800 (1999)

    Article  ADS  Google Scholar 

  37. Albrecht, T. & Levermann, A. Fracture field for large-scale ice dynamics. J. Glaciol. 58, 165–176 (2012)

    Article  ADS  Google Scholar 

  38. 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 

  39. Bueler, E. D., 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 

  40. Gomez, N., Pollard, D., Mitrovica, J. X., Huybers, P. & Clark, P. U. Evolution of a coupled marine ice sheet–sea level model. J. Geophys. Res. 117, F01013 (2012)

    Article  ADS  Google Scholar 

  41. Lenaerts, J., van den Broeke, M., van de Berg, W., van Meijgaard, E. & Munneke, P. A new, high-resolution surface mass balance map of Antarctica (1979–2010) based on regional atmospheric climate modeling. Geophys. Res. Lett. 39, L04501 (2012)

    Article  ADS  Google Scholar 

  42. Comiso, J. Variability and trends in Antarctic surface temperatures from in situ and satellite infra-red measurements. J. Clim. 13, 1674–1696 (2000)

    Article  ADS  Google Scholar 

  43. Le Brocq, A., Payne, A. & Vieli, A. An improved Antarctic dataset for high resolution numerical ice sheet models (ALBMAP v1). Earth Syst. Sci. Data 2, 247–260 (2010)

    Article  ADS  Google Scholar 

  44. Thompson, S. L. & Pollard, D. Greenland and Antarctic mass balances for present and doubled atmospheric CO2 from the genesis version-2 global climate model. J. Clim. 10, 871–900 (1997)

    Article  ADS  Google Scholar 

  45. Pal, J. S. et al. Regional climate modeling for the developing world: the ICTP RegCM3 and RegCNET. Bull. Am. Meteorol. Soc. 88, 1395–1409 (2007)

    Article  ADS  Google Scholar 

  46. Martin, M. A., Levermann, A. & Winkelmann, R. Comparing ice discharge through West Antarctic Gateways: Weddell vs. Amundsen Sea warming. Cryosphere Discuss. 9, 1705–1733 (2015)

    Article  ADS  Google Scholar 

  47. Zickfeld, K. et al. Long-term climate change commitment and reversibility: an EMIC intercomparison. J. Clim. 26, 5782–5809 (2013)

    Article  ADS  Google Scholar 

  48. Frieler, K. et al. Consistent evidence of increasing Antarctic accumulation with warming. Nature Clim. Change 5, 348–352 (2015)

    Article  ADS  Google Scholar 

  49. Golledge, N. R., Fogwill, C. J., Mackintosh, A. N. & Buckley, K. M. Dynamics of the Last Glacial Maximum Antarctic ice-sheet and its response to ocean forcing. Proc. Natl Acad. Sci. USA 109, 16052–16056 (2012)

    Article  ADS  CAS  Google Scholar 

  50. Golledge, N. et al. Antarctic contribution to meltwater pulse 1A from reduced Southern Ocean overturning. Nature Commun. 5, 1–10 (2014)

    Article  Google Scholar 

  51. Pollard, D. & DeConto, R. M. A simple inverse method for the distribution of basal sliding coefficients under ice sheets, applied to Antarctica. Cryosphere 6, 953–971 (2012)

    Article  ADS  Google Scholar 

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

    Article  ADS  Google Scholar 

  53. Durand, G., Gagliardini, O., Zwinger, T., Le Meur, E. & Hindmarsh, R. C. Full Stokes modeling of marine ice sheets: influence of the grid size. Ann. Glaciol. 50, 109–114 (2009)

    Article  ADS  Google Scholar 

  54. Pattyn, F. et al. Grounding-line migration in plan-view marine ice-sheet models: results of the ice2sea MISMIP3d intercomparison. J. Glaciol. 59, 410–422 (2013)

    Article  ADS  Google Scholar 

  55. Dutrieux, P. et al. Pine Island glacier ice shelf melt distributed at kilometre scales. Cryosphere 7, 1543–1555 (2013)

    Article  ADS  Google Scholar 

  56. Naish, T. & Zwartz, D. Palaeoclimate: looking back to the future. Nature Clim. Change 2, 317–318 (2012)

    Article  ADS  Google Scholar 

  57. Graversen, R. G. & Wang, M. Polar amplification in a coupled climate model with locked albedo. Clim. Dyn. 33, 629–643 (2009)

    Article  Google Scholar 

  58. Masson-Delmotte, V. et al. in Climate Change 2013: The Physical Science Basis. Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change (eds Stocker, T . et al.) 383–464 (2013)

    Google Scholar 

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

    Article  ADS  CAS  Google Scholar 

Download references

Acknowledgements

We thank the CMIP community for making their data openly available, and J. Lenaerts for providing present-day surface mass balance data. We are also grateful to K. Buckley (Victoria University high-performance computing cluster), C. Khroulev, T. Albrecht and the Parallel Ice Sheet Model groups at the University of Alaska, Fairbanks, and the Potsdam Institute for Climate Impact Research. This work was funded by contract VUW1203 of the Royal Society of New Zealand’s Marsden Fund, with support from the Antarctic Research Centre, Victoria University of Wellington, ANDRILL, GNS Science (NZ Ministry of Business Innovation and Employment contract C05X1001), National Science Foundation grant ANT-1043712, and the Australian Research Council (ARC). J. Renwick and D. Zwartz provided comments that improved the manuscript.

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Authors and Affiliations

Authors

Contributions

N.R.G. devised and carried out the ice-sheet modelling experiments and D.E.K. undertook climate model simulations to produce the present-day ocean temperature field. All authors contributed to the development of ideas and writing of the manuscript.

Corresponding author

Correspondence to N. R. Golledge.

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The authors declare no competing financial interests.

Extended data figures and tables

Extended Data Figure 1 CMIP5 multi-model ensemble mean anomaly timeseries data.

Air temperature (a–d), precipitation (e–h) and ocean temperature (i–l) changes for four RCP scenarios expressed as perturbations from present, both for hemispheric sectors and for the global mean.

Source data

Extended Data Figure 2 Long-term RCP temperature scenarios.

Antarctic-specific (60°–90° S) projected temperature trends to 2300 ce based on CMIP5 values at 2100 ce and extended to 2300 ce following trajectories of global means from intermediate-complexity Earth system models3,47. Precipitation and ocean temperature trends are calculated to follow those of atmospheric temperatures, with magnitudes based on analysis of the CMIP5 data set indicating a 5.3% increase in precipitation per degree air temperature increase and a ratio of 0.25 for converting atmospheric to oceanic temperature changes. dT, change in air temperature.

Source data

Extended Data Figure 3 Model spin-up and fit to present-day.

Ice-sheet geometry and surface velocities (ma-1, metres per year) at the end of a 25,000-year evolutionary simulation. a and b, Observation-based52 (a) and modelled (b) ice-sheet extent and surface elevations. c, Comparison of ice thicknesses shown in a and b. d and e, Measured59 (d) and modelled (e) surface ice velocities. f, Comparison of the ice velocities shown in d and e. ‘MeASURES’ is the name of the published ice velocity dataset of ref. 59.

Extended Data Figure 4 Multi-millennial changes in ice-sheet volume and area.

Simulated changes in ice-sheet volume (a) and ice-sheet area (b) under single-parameter and combined forcings (ΔTair, ΔPeff and ΔSST), based on simplified RCP scenarios for 100-year and 300-year forcing periods. Also shown in both panels is the control experiment (thick blue lines), illustrating little to no drift during the period of interest to 5000 ce.

Source data

Extended Data Figure 5 Multi-millennial changes in ice-sheet response to single-parameter environmental forcings.

Bias-corrected rates of sea-level-equivalent ice-mass change (s.l.e. mm a-1, millimetres of sea level equivalent per year) for each of the single-parameter simplified RCP forcing experiments. a, Rates of change under applied air temperature forcings peak at around 2240–2330 ce for both the 100-year and 300-year forcing experiments and decline thereafter, but both the 100-year and 300-year experiments exhibit rates that are still much larger than initial values by 5000 ce. b, Ice-mass rates of change as in a but forced only with precipitation changes. Maxima for the 100-year and 300-year forcing experiments occur close to the end of the forcing period, reflecting little inherent lag. c, Rates of change in response to ocean forcing show much more elevated initial peaks compared to mass-loss rates in subsequent millennia. By the end of the run, rates of mass loss for both the 100-year and 300-year forcing experiments are still higher than at the beginning of the run. Data are shown relative to zero at 2000 ce.

Source data

Extended Data Figure 6 Model sensitivity and uncertainties.

a, Modelled ice volume changes relative to the control run (in sea-level equivalent) for simulations in which only the grounding-line parameterization is altered. ‘SG’ and ‘Slip’ denote respectively the sub-grid and reduced traction grounding-line schemes employed in our simulations; ‘no SGmelt’ indicates an experiment in which only the sub-grid basal melt interpolation scheme is turned off (see Methods for details). Grey shading denotes period of applied forcing. b and c, Domain-integrated grounded (gr.) ice area (b) and sea-level-equivalent ice volume (c) trajectories under RCP 8.5 conditions for simulations in which the full sub-grid scheme is used and only the model resolution is changed. The 5-km simulation was not run beyond 3100 ce owing to the large computational overhead. d, Grounding-line positions at 2500 ce for the experiments shown in b and c. The greatest differences occur in the Siple Coast area (SC). Note the very close agreement between the 10-km and 5-km simulations. eg, Grounding-line locations under RCP 8.5 conditions at 2100 ce (e), 2300 ce (f) and 5000 ce (g) for experiments using the full grounding-line parameterization (‘SG+Slip’) compared to those in which the sub-grid basal melt interpolation is turned off (‘no SGmelt’). hj, Grounding-line locations under RCP 8.5 conditions at 2100 ce (j), 2300 ce (i) and 5000 ce (j) for 10-km and 20-km simulations that use the full grounding-line parameterization and resolution-specific stress balance tunings.

Source data

Extended Data Figure 7 The effect of polar amplification.

a, Geometry of the modelled Antarctic ice sheets under RCP 8.5 at 5000 ce, using both variants of the grounding-line scheme. Bold values and those in italics denote magnitudes and rates of sea-level contributions respectively. Leading values and those in parentheses relate to ‘low’ and ‘high’ scenarios respectively. Panels show ice extent for ‘low’ simulations; blue lines show grounding-line locations for ‘high’ simulations. Pale blue shading shows grounded ice lost in ‘high’ simulations but present in the ‘low’ scenario. b, Duplicate simulation to a but using a 2 × amplification of Antarctic temperatures beyond 2300 ce. Note the greater sea-level contribution compared to a. c, The full equilibrium response of the polar amplification scenario shown in b. Note the greater loss of ice from the Wilkes Basin (WB) and eastern Weddell Sea (WS), resulting in a higher total sea-level contribution. Black areas denote ice-free land. d, Rate of ice loss for the 2 × amplification scenario for ‘low’ (black) and ‘high’ (blue) scenarios, illustrating that although the fastest contribution to sea level (2–4 m per century) occurs during the first millennium, slower mass loss continues for many millennia thereafter.

Source data

Extended Data Figure 8 Antarctic contribution to GMSL.

a, Predicted sea-level contribution from the AIS for ‘high’ and ‘low’ simulations (coloured lines) under each of the four RCP scenarios as well as one that includes 2 × amplification of Antarctic temperatures by 2300 ce (darker shading), based on coeval climatic and oceanic perturbations. The forced response (grey shading) represents 20% to 42% of the committed response by 5000 ce. Lighter shading between coloured lines shows rates of sea-level-equivalent ice loss for each scenario. b, Long-term sea-level commitment as a function of atmospheric warming (blue shading with squares). Intermediate response curves for the ‘low’ simulations are shown in dotted lines. Red shading with triangles shows relationship between ice-shelf area and atmospheric warming for the near-equilibrium response and for intermediate stages (dotted lines). All curves in b are based on data from the four RCP scenario simulations, as well as one that includes 2 × amplification of Antarctic temperatures by 2300 ce, and two additional experiments whose maximum air temperature forcings are 1.5 °C and 3.35 °C. Pink shading defines the temperature range within which an ice-shelf extent less than 50% of present is simulated.

Source data

Extended Data Table 1 CMIP5 multi-model ensemble mean environmental perturbations
Extended Data Table 2 Parameter values found to best reproduce present-day Antarctic ice-sheet configuration

Supplementary information

Modelled ice sheet evolution under Antarctic-specific RCP 8.5 warming scenario

Main graphic shows ice extent for 'low' simulations; blue lines show grounding-line locations for 'high' simulations. Pale blue shading shows grounded ice lost in 'high' simulations but present in the 'low' scenario. Grey shading denotes ice shelves. Note the increasing divergence between 'high' and 'low' beyond 2300 CE. Bold values and those in italics denote magnitudes and rates of sea-level contributions respectively. Leading values and those in parentheses relate to 'low' and 'high' scenarios respectively. WAIS: West Antarctic Ice Sheet; EAIS: East Antarctic Ice Sheet. (MP4 6204 kb)

Modelled ice sheet evolution under Antarctic-specific RCP 8.5 warming scenario

Main graphic shows ice extent for 'high' simulations. Warmer colours indicate areas of relatively faster-flowing ice. WAIS: West Antarctic Ice Sheet; EAIS: East Antarctic Ice Sheet. Graph shows the Antarctic contribution to global sea-level. (MP4 5638 kb)

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Golledge, N., Kowalewski, D., Naish, T. et al. The multi-millennial Antarctic commitment to future sea-level rise. Nature 526, 421–425 (2015). https://doi.org/10.1038/nature15706

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