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Researchers monitor Antarctica’s hidden ice system by combining satellite observations with measurements made on, through, and beneath the ice. Satellites track broad patterns in ice motion, surface height, fractures, and shelf edges; field radar and seismic surveys reveal ice thickness and the bed or seafloor; and borehole sensors, ocean instruments, and under-ice vehicles sample water directly. No single method observes every part of the system.
What “beneath the ice” can mean
The phrase can refer to different layers and boundaries: internal layers within the ice, the ice base, water flowing beneath a floating ice shelf, the grounding zone where grounded glacier ice begins to float, or the bedrock and seafloor below. Researchers choose instruments according to which part they need to observe and what quantity they need to measure.
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Some observations are direct, such as a sensor measuring water temperature in a borehole. Others are indirect: a satellite measures surface elevation or motion, and researchers use those data with other measurements to infer what may be happening below. A surface-height change alone, for example, does not identify its cause.
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Ice shelves are floating extensions of land ice, with the atmosphere above and ocean below. Ocean interaction can melt the underside and contribute to shelf thinning, as the Australian Antarctic Program explains. Because the ice and the water affect one another, researchers combine measurements of both.
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Which instruments reveal which parts of the system?
| Method | What it measures or reveals | Coverage and limits |
|---|---|---|
| Satellite synthetic aperture radar (SAR) | Repeated radar images show surface texture, crevasses, ice motion, and change over broad areas. NASA/JPL’s NISAR reporting describes radar observations that reveal properties distinct from optical imagery and shows glacier flow around a nunatak. | Radar can work through cloud and, depending on wavelength and conditions, reveal features beneath snow or near the surface. It does not automatically produce a complete picture of everything beneath thick ice; researchers pair it with elevation data and field measurements. |
| Satellite laser altimetry | Measures surface elevation. Comparing measurements over time helps identify thinning or thickening. NASA describes using tidal flexure—the rise and fall of floating ice with the tide—to help distinguish floating shelf from grounded ice. | Provides broad observations, but a height change can have more than one cause. Researchers interpret it alongside ice-flow and other satellite data. |
| Optical and thermal-infrared imagery | Optical images map visible features; thermal-infrared observations show temperature-related patterns. NASA describes combining visible, thermal-infrared, and radar imagery with ice-flow information to map ice-shelf edges. | Clouds, illumination, and visual similarities among snow, ice, and clouds can complicate interpretation. Multiple sensor types help distinguish features. |
| GPS stations | Fixed stations measure ice motion and surface elevation. A network can track local flow and deformation. | Measurements are local to station locations, so researchers use GPS alongside satellites for regional context. |
| Ground-penetrating and ice-penetrating radar | Radio waves sent into ice help estimate thickness and image internal layers or the ice-bed interface. Airborne radar surveys can map hidden basins and bed structure. Phase-sensitive radar such as ApRES can detect small changes in ice thickness over time. | What radar can detect depends on instrument design and the material it must cross. The Australian Antarctic Program notes ApRES cannot penetrate salt water: it measures ice thickness, not the water cavity beneath it. |
| Seismic surveys | Sound waves help investigate ice structure, cavity geometry, water layers, grounding zones, and seafloor bathymetry. British Antarctic Survey and Australian Antarctic Program accounts describe seismic measurements used alongside radar and GPS. | Surveys are usually localized and logistically demanding. Their results are interpreted with radar and ocean measurements. |
| Borehole and ocean instruments | Temperature sensors, pressure transducers, current profilers, and moorings measure conditions in ice and water beneath shelves, including water temperature and flow speed. | They provide direct measurements at deployment sites and during the instruments’ operating period, rather than satellite-scale coverage. |
| Autonomous under-ice vehicle | Icefin carries instruments including temperature and conductivity sensors, a current profiler, camera, oxygen sensor, and multibeam echosounder. It can observe water and an ice shelf’s underside through a borehole. | It provides detailed local observations, not continent-wide coverage. British Antarctic Survey’s MELT project page describes the project from 2018 to 2023; it is an example of the approach, not evidence of a current deployment. |
How the measurements work together
- Locate change across a region. Satellite radar and optical imagery help map ice motion, fractures, and changing shelf edges. NASA/JPL reported that public access to NISAR L-band and S-band data began on July 20, 2026, and said the mission teams were processing and releasing data. That report does not establish a fixed current revisit cadence.
- Measure surface-height change. Satellite laser altimetry records elevation over time. Researchers compare it with motion and other observations to assess whether a shelf or glacier is thinning or thickening and to help identify whether ice is floating.
- Check regional patterns at field sites. GPS stations provide local motion and elevation records that can be compared with satellite measurements.
- Map the ice interior and its base. Ground or airborne radar estimates ice thickness and reveals internal layers or the ice-bed interface. The Australian Antarctic Program also describes airborne surveys combining ice-penetrating radar with gravity, magnetometer, laser-altimeter, and GPS measurements to investigate hidden structure.
- Investigate below the ice or cavity. Where ice-only radar cannot cross salt water, seismic surveys can help map water layers, cavity geometry, grounding zones, and the seafloor.
- Sample the ocean directly. Borehole sensors, moorings, and under-ice vehicles record local water conditions, including temperature and currents. Researchers compare those observations with ice measurements and models of ice flow and ocean circulation.
The method mix is important: satellites offer repeated views over broad regions, while field instruments provide more direct, detailed observations at specific locations. Models help connect the two, but a model-based interpretation is not the same thing as a direct measurement of the hidden water or bed.
Independent reader supportYour contribution helps us test, update, and keep practical guides available for everyone.Why grounding lines are closely watched
A grounding line marks where a glacier or ice sheet loses contact with the bed and begins to float. Its position matters because changes there can indicate that the boundary between grounded ice and floating shelf is shifting. NASA’s account of research on Smith, Pope, and Kohler glaciers describes using satellite radar data to trace grounding-line change.
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In that study, Smith Glacier’s grounding line retreated at a reported rate of 1.24 miles (2 kilometres) per year since 1996. That figure applies to Smith Glacier and the study’s stated period; it is not an Antarctic-wide rate.
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What the observations can—and cannot—establish
- Broad patterns are not the same as a complete under-ice image. Satellite radar and altimetry show surface properties and change over large areas; field radar, seismic work, and ocean instruments help resolve what lies below.
- Direct ocean readings are spatially limited. A borehole, mooring, or vehicle can measure conditions at its location and during its deployment, while satellites provide broader context.
- Different signals answer different questions. Ice thickness, surface elevation, flow speed, water temperature, and seafloor shape are distinct quantities, so researchers combine instruments rather than treating any one reading as a full account of change.
- Campaigns have specific dates. For example, the British Antarctic Survey MELT project page covers 2018–2023, and the Australian Antarctic Program’s Sørsdal Glacier account describes planned deployments for the 2016–17 season. These illustrate methods, not current deployments.
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