Potential sea-level rise from Antarctic ice-sheet instability constrained by observations

Journal name:
Nature
Volume:
528,
Pages:
115–118
Date published:
DOI:
doi:10.1038/nature16147
Received
Accepted
Published online

Large parts of the Antarctic ice sheet lying on bedrock below sea level may be vulnerable to marine-ice-sheet instability (MISI)1, a self-sustaining retreat of the grounding line triggered by oceanic or atmospheric changes. There is growing evidence2, 3, 4 that MISI may be underway throughout the Amundsen Sea embayment (ASE), which contains ice equivalent to more than a metre of global sea-level rise. If triggered in other regions5, 6, 7, 8, the centennial to millennial contribution could be several metres. Physically plausible projections are challenging9: numerical models with sufficient spatial resolution to simulate grounding-line processes have been too computationally expensive2, 3, 10 to generate large ensembles for uncertainty assessment, and lower-resolution model projections11 rely on parameterizations that are only loosely constrained by present day changes. Here we project that the Antarctic ice sheet will contribute up to 30 cm sea-level equivalent by 2100 and 72 cm by 2200 (95% quantiles) where the ASE dominates. Our process-based, statistical approach gives skewed and complex probability distributions (single mode, 10 cm, at 2100; two modes, 49 cm and 6 cm, at 2200). The dependence of sliding on basal friction is a key unknown: nonlinear relationships favour higher contributions. Results are conditional on assessments of MISI risk on the basis of projected triggers under the climate scenario A1B (ref. 9), although sensitivity to these is limited by theoretical and topographical constraints on the rate and extent of ice loss. We find that contributions are restricted by a combination of these constraints, calibration with success in simulating observed ASE losses, and low assessed risk in some basins. Our assessment suggests that upper-bound estimates from low-resolution models and physical arguments9 (up to a metre by 2100 and around one and a half by 2200) are implausible under current understanding of physical mechanisms and potential triggers.

At a glance

Figures

  1. Projected grounding-line retreat.
    Figure 1: Projected grounding-line retreat.

    a, b, Probability density estimates of grounding-line retreat at 2100 (a) and 2200 (b), overlaid on bedrock topography24. Red lines show 0.05 contour: an estimated 95% probability that retreat will be less extensive than this. c, d, ASE with Pine Island (PIG) and Thwaites glaciers.

  2. Projected sea-level rise.
    Figure 2: Projected sea-level rise.

    a, Quantiles of Antarctic dynamic mass losses in cm sea-level equivalent as a function of time. b, Probability densities at 2100 and 2200. c, Probabilities of exceeding particular thresholds as a function of time. d, Probability of exceeding any threshold at 2100 and 2200.

  3. Projected rate of sea-level rise from the Amundsen Sea.
    Figure 3: Projected rate of sea-level rise from the Amundsen Sea.

    a, Quantiles of the rate of ASE dynamic mass losses in mm yr−1 sea-level equivalent (SLE) as a function of time. b, Probability densities at 2100 and 2200. c, Probabilities of exceeding particular thresholds as a function of time. d, Probability of exceeding any threshold at 2100 and 2200.

  4. Grounding-line retreat parameterization.
    Extended Data Fig. 1: Grounding-line retreat parameterization.

    a, Cumulative probability distributions of MISI onset for 14 basins (Fig. 1) aggregated into 11 independent sectors. b, Piecewise linear parameterization prescribing the dependence of grounding-line retreat rate on the logarithm of the effective basal friction coefficient (Extended Data Fig. 2). Each of the 1,000 functional forms is a variant used in the ensemble; a subset are shown in bold as examples. See also Supplementary Information, sections 1.6.1, 1.6.2.

  5. Initialization and basal friction evolution.
    Extended Data Fig. 2: Initialization and basal friction evolution.

    ac, Initial values of the difference between simulated and observed surface elevation (a); velocities averaged over ice thickness (b); the logarithm of the initial effective basal friction coefficient, α = log10(β1′ (x; t = t0)) (c). d, As for c, showing the ASE. e, As for d, at 2200 in the plastic sliding law ensemble member that best matches present day ASE observations. See also Supplementary Information, section 1.5.

  6. Projected grounding-line retreat and initial basal friction.
    Extended Data Fig. 3: Projected grounding-line retreat and initial basal friction.

    a, b, Initial grounding line and map of α values (Extended Data Fig. 2) with retreat probability contours at 2200 for the Weddell Sea sector (a) and ASE (b): for example, there is an estimated 33% probability that grounding-line retreat will be less extensive than the 66% contour.

  7. Ice dynamical conditions for retreat.
    Extended Data Fig. 4: Ice dynamical conditions for retreat.

    ac, Surface elevation changes at 2200 in the ensemble member with maximum sea-level contribution at 2200 (plastic sliding law): standard settings (a); ‘Schoof flux’ condition off, thereby only allowing grounding-line retreat along strictly downsloping bedrock (b); ‘no suction’ check off, thereby allowing thinning due to grounding line retreat to occur faster than the theoretical limit (c). See also Supplementary Information, section 2.2.1.

  8. Relationship between present and future sea-level contributions from the Amundsen Sea.
    Extended Data Fig. 5: Relationship between present and future sea-level contributions from the Amundsen Sea.

    a, b, Dynamic mass losses in cm sea-level equivalent from the ASE at 2100 (a) and 2200 (b), as a function of present day mass loss in the same region. The branches arise from interactions between basal drag coefficient and friction law that produce different rates of, and impediments to, grounding-line retreat. The observed mass loss is shown, along with observational (± 3σo) and total (± 3σt) uncertainties (Supplementary Information, section 1.7).

  9. Contributions of each basal friction law.
    Extended Data Fig. 6: Contributions of each basal friction law.

    a, b, Probability distributions of Antarctic dynamic mass losses in cm sea-level equivalent at 2100 (a) and 2200 (b) (as in Fig. 2b), showing the cumulative contributions of the basal friction laws.

  10. Uncalibrated projections.
    Extended Data Fig. 7: Uncalibrated projections.

    ah, Prior (uncalibrated) projections of Antarctic dynamic mass losses in cm sea-level equivalent (ad); rate of ASE dynamic mass losses in mm yr−1 sea-level equivalent (SLE) (eh). Posterior (calibrated) projections are in Figs 2 and 3. See also Supplementary Information, section 1.7.

  11. Parameter calibration and influence.
    Extended Data Fig. 8: Parameter calibration and influence.

    a, b, Weights for each of the 1,000 sub-ensemble parameter sets (averaged over basal friction laws) as a function of low threshold of effective basal drag coefficient (αlow) and maximum retreat rate (vmax) (a); bedrock map index and high threshold of effective basal drag coefficient (αhigh) (b). Darker colours indicate values favoured by observational calibration. c, d, Uncalibrated dynamic mass losses at 2200 in cm sea-level equivalent (SLE) as functions of the same.

  12. Sensitivity to retreat onset distributions.
    Extended Data Fig. 9: Sensitivity to retreat onset distributions.

    ad, Projections at 2200 estimated for four individual basins under different retreat onset scenarios. a, ASE: original; ‘probability × 0.8’, in which 20% of simulations are set to zero contribution; ‘late retreat’, in which all simulations begin retreating between 2020 and 2030; and ‘early retreat’, retreating between 2000 and 2010; b, Shackleton; c, Siple Coast; and d, Transantarctic Mountains: original, and onset probabilities adjusted by the factors shown. See also Supplementary Information, section 2.2.2.

  13. Sensitivity tests for plastic sliding law.
    Extended Data Fig. 10: Sensitivity tests for plastic sliding law.

    Antarctic dynamic mass losses in cm sea-level equivalent under various conditions: ‘Max likelihood’, the plastic simulation that best matches present day ASE observations; ‘Uncalib 95%’ and ‘Calib 95%’, the plastic quantiles before and after calibration, respectively, and ‘Calib ASE 95%’, the estimate calibrating only the ASE; ‘Ensemble max’, the simulation with highest contribution at 2200; ‘Extreme onset’, the previous with all basins retreating from 2000 or 2020; ‘Max params’, the previous with retreat parameters at maximum values and ‘Extreme params’ at higher values; ‘Schoof flux’ and ‘No suction’ checks off (dashed to indicate that they are physically unrealistic). See also Supplementary Information, sections 2.2, 2.3.

Videos

  1. Animation of the Amundsen Sea Embayment
    Video 1: Animation of the Amundsen Sea Embayment
    Summary of the projections in ten-year time steps. The black contour shows the projected median grounding line position. The map shows the mean change in surface elevation, with -100 m contour shown in green. Dashed purple lines show the borders of Pine Island Glacier (PIG) and Thwaites Glacier, which together comprise the Amundsen Sea Embayment.

References

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  2. Favier, L. et al. Retreat of Pine Island Glacier controlled by marine ice-sheet instability. Nature Clim. Chang. 5, 15 (2014)
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Author information

  1. These authors contributed equally to this work.

    • Catherine Ritz &
    • Tamsin L. Edwards

Affiliations

  1. CNRS, LGGE, F-38041 Grenoble, France

    • Catherine Ritz,
    • Gaël Durand &
    • Vincent Peyaud
  2. Université Grenoble Alpes, LGGE, F-38041 Grenoble, France

    • Catherine Ritz,
    • Gaël Durand &
    • Vincent Peyaud
  3. Department of Environment, Earth and Ecosystems, Faculty of Science, The Open University, Walton Hall, Milton Keynes, MK7 6AA, UK

    • Tamsin L. Edwards
  4. Department of Geographical Sciences, University of Bristol, University Road, Bristol BS8 1SS, UK

    • Tamsin L. Edwards &
    • Antony J. Payne
  5. British Antarctic Survey, Natural Environment Research Council, Madingley Road, Cambridge CB3 0ET, UK

    • Richard C. A. Hindmarsh

Contributions

C.R. and V.P. worked on the development of the GRISLI model and did the numerical modelling. C.R. and G.D., with contributions from T.L.E., performed the physics analysis. T.L.E. designed the experiments with contributions from all authors, wrote the manuscript with contributions from C.R. and G.D., and performed the statistical analysis. T.L.E. and C.R. produced the figures and animation, with contributions from G.D. The sampling and geostatistical analysis were produced by A.J.P., and the theoretical conditions of grounding-line retreat were developed by R.A.H., C.R. and G.D.

Competing financial interests

The authors declare no competing financial interests.

Corresponding author

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Author details

Extended data figures and tables

Extended Data Figures

  1. Extended Data Figure 1: Grounding-line retreat parameterization. (532 KB)

    a, Cumulative probability distributions of MISI onset for 14 basins (Fig. 1) aggregated into 11 independent sectors. b, Piecewise linear parameterization prescribing the dependence of grounding-line retreat rate on the logarithm of the effective basal friction coefficient (Extended Data Fig. 2). Each of the 1,000 functional forms is a variant used in the ensemble; a subset are shown in bold as examples. See also Supplementary Information, sections 1.6.1, 1.6.2.

  2. Extended Data Figure 2: Initialization and basal friction evolution. (723 KB)

    ac, Initial values of the difference between simulated and observed surface elevation (a); velocities averaged over ice thickness (b); the logarithm of the initial effective basal friction coefficient, α = log10(β1′ (x; t = t0)) (c). d, As for c, showing the ASE. e, As for d, at 2200 in the plastic sliding law ensemble member that best matches present day ASE observations. See also Supplementary Information, section 1.5.

  3. Extended Data Figure 3: Projected grounding-line retreat and initial basal friction. (828 KB)

    a, b, Initial grounding line and map of α values (Extended Data Fig. 2) with retreat probability contours at 2200 for the Weddell Sea sector (a) and ASE (b): for example, there is an estimated 33% probability that grounding-line retreat will be less extensive than the 66% contour.

  4. Extended Data Figure 4: Ice dynamical conditions for retreat. (433 KB)

    ac, Surface elevation changes at 2200 in the ensemble member with maximum sea-level contribution at 2200 (plastic sliding law): standard settings (a); ‘Schoof flux’ condition off, thereby only allowing grounding-line retreat along strictly downsloping bedrock (b); ‘no suction’ check off, thereby allowing thinning due to grounding line retreat to occur faster than the theoretical limit (c). See also Supplementary Information, section 2.2.1.

  5. Extended Data Figure 5: Relationship between present and future sea-level contributions from the Amundsen Sea. (559 KB)

    a, b, Dynamic mass losses in cm sea-level equivalent from the ASE at 2100 (a) and 2200 (b), as a function of present day mass loss in the same region. The branches arise from interactions between basal drag coefficient and friction law that produce different rates of, and impediments to, grounding-line retreat. The observed mass loss is shown, along with observational (± 3σo) and total (± 3σt) uncertainties (Supplementary Information, section 1.7).

  6. Extended Data Figure 6: Contributions of each basal friction law. (206 KB)

    a, b, Probability distributions of Antarctic dynamic mass losses in cm sea-level equivalent at 2100 (a) and 2200 (b) (as in Fig. 2b), showing the cumulative contributions of the basal friction laws.

  7. Extended Data Figure 7: Uncalibrated projections. (425 KB)

    ah, Prior (uncalibrated) projections of Antarctic dynamic mass losses in cm sea-level equivalent (ad); rate of ASE dynamic mass losses in mm yr−1 sea-level equivalent (SLE) (eh). Posterior (calibrated) projections are in Figs 2 and 3. See also Supplementary Information, section 1.7.

  8. Extended Data Figure 8: Parameter calibration and influence. (917 KB)

    a, b, Weights for each of the 1,000 sub-ensemble parameter sets (averaged over basal friction laws) as a function of low threshold of effective basal drag coefficient (αlow) and maximum retreat rate (vmax) (a); bedrock map index and high threshold of effective basal drag coefficient (αhigh) (b). Darker colours indicate values favoured by observational calibration. c, d, Uncalibrated dynamic mass losses at 2200 in cm sea-level equivalent (SLE) as functions of the same.

  9. Extended Data Figure 9: Sensitivity to retreat onset distributions. (265 KB)

    ad, Projections at 2200 estimated for four individual basins under different retreat onset scenarios. a, ASE: original; ‘probability × 0.8’, in which 20% of simulations are set to zero contribution; ‘late retreat’, in which all simulations begin retreating between 2020 and 2030; and ‘early retreat’, retreating between 2000 and 2010; b, Shackleton; c, Siple Coast; and d, Transantarctic Mountains: original, and onset probabilities adjusted by the factors shown. See also Supplementary Information, section 2.2.2.

  10. Extended Data Figure 10: Sensitivity tests for plastic sliding law. (282 KB)

    Antarctic dynamic mass losses in cm sea-level equivalent under various conditions: ‘Max likelihood’, the plastic simulation that best matches present day ASE observations; ‘Uncalib 95%’ and ‘Calib 95%’, the plastic quantiles before and after calibration, respectively, and ‘Calib ASE 95%’, the estimate calibrating only the ASE; ‘Ensemble max’, the simulation with highest contribution at 2200; ‘Extreme onset’, the previous with all basins retreating from 2000 or 2020; ‘Max params’, the previous with retreat parameters at maximum values and ‘Extreme params’ at higher values; ‘Schoof flux’ and ‘No suction’ checks off (dashed to indicate that they are physically unrealistic). See also Supplementary Information, sections 2.2, 2.3.

Supplementary information

Video

  1. Video 1: Animation of the Amundsen Sea Embayment (2.58 MB, Download)
    Summary of the projections in ten-year time steps. The black contour shows the projected median grounding line position. The map shows the mean change in surface elevation, with -100 m contour shown in green. Dashed purple lines show the borders of Pine Island Glacier (PIG) and Thwaites Glacier, which together comprise the Amundsen Sea Embayment.

PDF files

  1. Supplementary Information (788 KB)

    This file contains Supplementary Methods, a Supplementary Discussion, Supplementary Data information and additional references.

Excel files

  1. Supplementary Table (419 KB)

    This file contains sea level projections.

Zip files

  1. Supplementary Data (8.8 MB)

    This zipped file contains R script and data: projections. The Code to output annual Antarctic posterior projections as the following options: modes (cm SLE), quantiles (cm SLE) or probabilities of non-exceedance (%) for any quantile/threshold and date range. These results correspond to the columns ‘Prob’ (probabilities of non-exceedance) and ‘SLE’ (modes, quantiles) for rows ‘ALL ANT Post’ in the Excel file, but using this script any quantile/threshold and year may be chosen.

Additional data