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Observations support faster calving from the tallest ice cliffs, but they do not show a self-sustaining marine ice-cliff instability (MICI). A dataset of 15,330 cliffs around Greenland and Antarctica finds that cliffs higher than 100 metres are uncommon and can calve at rates up to three times higher than existing model parameterizations. Retreat nevertheless tends to lose momentum as dynamic thinning reduces cliff height and ice flows into regions with smaller thickness gradients.
What the largest ice-cliff survey measured
A 15,330-cliff observational dataset
Needell, Walker and Bassis compiled measurements for 15,330 ice cliffs along the margins of Greenland and Antarctica. The work combines laser altimetry, optical imagery, airborne observations and historical records, allowing cliff geometry and calving behaviour to be compared across many environments rather than inferred from a single glacier.
Cliff height is not an isolated property in these observations. It is strongly correlated with mélange thickness, water depth and crevassing. Mélange is the mixture of sea ice and icebergs that can occupy a glacier front; thicker mélange can buttress the terminus, while deeper water and heavier fracturing alter how readily a vertical face fails. Those correlations mean that a height-only rule cannot describe the full range of observed calving.
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Cliffs taller than 100 metres occur in multiple settings, but they form a small part of the measured population. The tallest faces calve faster than rates produced by existing parameterizations, with observed rates reaching as much as a factor of three above those schemes. The result is evidence that some models understate short-term calving from unusually high, heavily stressed cliffs; it is not evidence that every tall cliff will enter runaway retreat.
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| Observation or model quantity | What the evidence establishes | Qualification |
|---|---|---|
| Measured cliffs | 15,330 | Needell, Walker and Bassis dataset, 2026 |
| Cliff height | Cliffs above 100 m are rare but present | Observed across diverse Greenland and Antarctic settings |
| Calving-rate comparison | Up to 3 times higher than existing parameterizations | Reported for the tallest observed cliffs; not a universal rate |
| Older parameterization range | Approximately 0 to 3 km per year | Model-context ramp, not a universal observed calving speed |
Do observations show marine ice-cliff instability?
No. The 2024 review of ice-cliff instability states that MICI has not yet been directly observed. The survey constrains the cliff heights and calving rates that a credible model must reproduce, but it does not document a retreat sequence that becomes self-sustaining solely because a cliff exceeds a particular height.
This distinction matters. A cliff can experience a temporary acceleration in calving when it is high, deeply submerged, strongly crevassed or weakly buttressed. MICI is a stronger claim: successive calving would expose a new cliff that remains unstable, causing retreat to accelerate without requiring an external increase in forcing. The available observations do not establish that feedback as a persistent process in modern ice sheets.
Why cliff height alone cannot predict retreat
Several interacting controls determine whether a face fails, how large the resulting iceberg is and whether the terminus can maintain rapid retreat.
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| Control | How it affects stability or calving |
|---|---|
| Freeboard and total thickness | Set the geometry and gravitational stress of the exposed face; height is only one part of that geometry. |
| Thickness gradient | Controls how quickly ice becomes thinner inland or downstream. Retreat into a region with a smaller gradient reduces the tendency for each new cliff to be as tall as the previous one. |
| Water depth | Changes the submerged geometry and the forces acting at the front; deeper water can permit larger, more unstable faces. |
| Mélange thickness | Provides resistance or buttressing at the terminus. Loss of mélange support can increase calving, while persistent mélange can limit frontal motion. |
| Crevasse density and preexisting flaws | Provide pathways for cracks to grow. The size and evolution of flaws are especially difficult to measure and may vary through space and time. |
| Material deformation | Viscous deformation can relax stress, while brittle tensile failure and shear-band formation can localize damage and trigger fracture. |
| Ocean and atmospheric forcing | Influence melt, mélange conditions, stress and the rate at which a terminus is driven toward retreat. |
The unresolved size and evolution of preexisting flaws is particularly important. Two cliffs with similar measured heights can have different failure risks if one contains a large connected fracture system and the other does not.
What stops a runaway sequence?
Dynamic thinning lowers the next cliff
As an outlet glacier accelerates and thins, the ice front can lose the thickness needed to sustain an exceptionally high face. The next cliff is therefore not guaranteed to inherit the height or stress state of the previous one.
Retreat can enter a gentler thickness gradient
Observed retreat may move the terminus into ice where thickness changes less sharply with distance. In that geometry, each step inland produces less additional gravitational driving stress, suppressing continued cliff growth.
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Resistance changes with the terminus environment
Mélange, bed geometry, viscous flow and fracture development can all change during retreat. Increased resistance or stress relaxation can interrupt an acceleration, while loss of buttressing can briefly intensify it. The observed system is therefore a sequence of competing feedbacks, not a height-triggered switch.
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How to judge a marine-ice-cliff model
A useful parameterization should be tested against the full observed population, not tuned to one dramatic terminus. The following checks separate a model that reproduces data from one that merely produces rapid retreat in a convenient scenario:
- Test the geometry. Include cliff height, freeboard, total thickness, thickness gradients and bed overdeepening.
- Represent fracture state. Account for crevasse density, preexisting flaw size, tensile failure and possible shear-band formation.
- Include forcing and resistance. Represent water depth, mélange thickness, ocean and atmospheric forcing, viscous deformation and buttressing.
- Validate across regions. Compare predicted cliff populations and calving rates with observations from both Greenland and Antarctica.
- Separate acceleration from runaway retreat. A model should report whether it produces a temporary calving pulse or a self-sustaining retreat that continues after external forcing is held constant.
The 15,330-cliff dataset provides a broad benchmark for the first four tests. It cannot, by itself, prove the fifth, because a distribution of cliff heights is not a direct observation of a multi-year, self-sustaining instability.
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What the findings mean for sea-level projections
The results justify revisiting how models represent the tallest cliffs: their calving can exceed older parameterizations by up to threefold. They do not justify translating that factor directly into a future sea-level contribution. Sea-level projections also depend on ice thickness, grounding-line migration, basin geometry, flow speed, melt and the duration of any acceleration.
The central evidence supports a conditional conclusion. High cliffs can calve unusually quickly, but the observed feedbacks that promote thinning, reduce thickness gradients or restore resistance can limit the duration of that acceleration. A projection that assumes every retreating cliff remains tall and unstable would go beyond what observations establish.
What researchers still need to resolve
Future tests need to connect short-term cliff measurements with the evolution of fractures, mélange and flow over longer periods. The 2024 Annual Reviews assessment calls for theories of iceberg calving, ice-shelf demise and ice-cliff instability to be tested across modern and paleo environments and a wide range of environmental and glaciological conditions.
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“Theories of iceberg calving, ice shelf demise, and ice cliff instability must now be fully tested against a wide range of environmental and glaciological conditions in both modern and paleo conditions.” — Annual Reviews review, 2024
Until those tests are available, the strongest empirical statement is narrower than a runaway-instability scenario: the tallest cliffs are real, their calving can outpace established parameterizations, and their retreat is moderated by geometry, fracture state, material deformation and changing environmental resistance.
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