AIRETH (Fig. b–c) is a dual-polarization, helicopter-borne GPR system designed for glaciological surveys that has been used extensively in the European Alps . Our Greenland campaign was conceived as a first deployment under polar conditions and as the first description of the current, redesigned AIRETH configuration. It aimed to assess whether AIRETH can provide measurements in polythermal, fast-flowing and crevassed outlet-glacier terrain.

AIRETH comprises a lightweight modular airframe carrying two commercial PulseEkko radar systems (Sensors & Software). At the core of the system are two orthogonal bistatic dipole antenna pairs operating at central frequencies of 25, 50, or 100 MHz. The radar hardware is controlled by a commercial central unit (SPIDAR pulseEkko Pro NIC-500P) and complemented by an integrated positioning and attitude system composed of (i) four GNSS antennas mounted at the frame corners, (ii) a central inertial measurement unit, and (iii) a laser altimeter providing ground-clearance information (Fig. c). System status and acquisition are monitored in real time from the helicopter cockpit.

Compared to earlier AIRETH configurations , the system has been substantially redesigned to improve robustness, positioning and data quality: the original wooden carrier frame was replaced by fibreglass-reinforced plastic beams, reducing total weight by about 60 % (now at 115 kg); the positioning system was integrated to retrieve platform position and orientation during flight; and cable routing was optimized to reduce electromagnetic noise in the GPR signal. Together, these changes yield a self-contained, modular platform and reduced operational constraints. A detailed hardware description of the current AIRETH configuration is provided in Supplement Fig. S1.

The surveys took place in March 2025, deploying AIRETH in the 25 MHz configuration to maximize the penetration depth. Data were acquired at a target altitude of 30 m above ground, with typical speeds of ∼ 35 km h⁻¹ on across-glacier profiles and ∼ 55 km h⁻¹ on longitudinal profiles. The few intersections of profiles with clear bed returns were used to assess continuity and internal consistency across individual survey lines. Overall, the collected dataset comprises a total of 348 km of survey lines, encompassing at least one longitudinal profile and several cross profiles for each glacier. The Matlab based GPRglaz package was used for data processing. It included two main steps: processing of the positioning data and processing of the GPR data. GNSS, IMU and laser-altimeter data were quality-controlled and combined to obtain platform positions, which were projected onto the glacier surface and synchronized with the GPR traces via GNSS timestamps.

The GPR data were processed following a standard processing workflow to improve signal–to–noise ratio and enable clear interpretation. Processing aims to extract the glacier bed reflections and estimate the ice thickness; it includes: (i) time zero correction based on the arrival of the direct wave, (ii) removal of the ringing noise from helicopter using singular value decomposition filtering, (iii) Butterworth bandpass filtering (10–75 MHz), (iv) trace binning at a constant spatial sampling rate of 1 m for regular sampling, (v) surface reflection picking based on the laser altimetry, (vi) merging the dual-polarization data channels, (vii) time-to-depth conversion by data migration (Kirchhoff and Reverse time migration algorithms), assuming constant radar wave velocities of 0.30 and 0.168 m ns⁻¹, for air and ice, respectively. The signal associated with the basal reflection was manually picked in the Petrel software environment (Schlumberger) and the ice thickness was computed as the difference between the elevation of the glacier surface and the elevation of the basal reflections.

In order to place our results into the context of existing information, we compare them with two available ice thickness and bed elevation constraints: NASA's OIB radar soundings and the BM mass-conservation inversion product . We assess the local consistency between AIRETH and existing constraints using point-wise comparisons at collocated locations.

For the comparison with OIB, we used the Level-2 radar product of . We converted the reported one-way surface and bottom ranges to elevations following . Since both datasets are referenced to the WGS-84 ellipsoid, no surface correction is required. For each AIRETH bed pick, we matched OIB soundings (along-track spacing 15 m) within a 10 m horizontal radius and, where multiple valid soundings existed, averaged their bed elevations. Unmatched points were discarded.

For BM comparison, we used BM v5 (NSIDC IDBMG4) from the NSIDC DAAC . We sampled its gridded bed, surface, thickness, and source index at each AIRETH bed-pick location. Within our study region, only 5.5 % of BM grid cells are reported as directly constrained by thickness measurements; the remaining 94.5 % rely on mass-conservation inversion and interpolation.

Bed reflections were identified along about 29 % (102 km out of 348 km) of the AIRETH flight lines, with most bed picks obtained in the Sermilik Bræ and Qooqqup Sermia areas (Fig. a). The spatial distribution of bed returns is biased towards shallower glacier margins, whereas bed picks are mainly absent in the thicker central glacier sections. This pattern indicates that basal reflections were most commonly detectable up to ice thicknesses of approximately 300 m, although deeper detections were obtained locally. Only about 5 % of bed picks correspond to ice thicknesses greater than 300 m, and the maximum detected ice thickness is approximately 340 m. At locations without interpretable bed returns, BM indicates thickness higher than 300 m in about 32 % of cases, predominantly along the longer longitudinal profiles. For glacier-scale context and to facilitate identification where bedrock was interpreted, Supplement Figs. S2 and S3 provide zoom-in maps for the glaciers highlighted in Fig. a. At some intersections between GPR profiles, a basal reflection is only interpretable along one of the crossing lines. This is not unexpected, because basal detectability depends on profile orientation relative to glacier geometry, as well as on local ice thickness, crevassing, clutter, and out-of-plane reflections from steep valley walls. Kirchhoff migration was applied using the same parameterization for all profiles, independent of survey orientation. However, because migration is applied along individual profiles, it may sharpen the imaging response preferentially in the along-track direction. Differences in flight speed between across-glacier and longitudinal survey modes, which result in different along-track trace densities prior to stacking, may further affect local signal quality and thus basal-reflection interpretability. As a result, the glacier bed may be interpretable along one profile but not along another, even at nearby crossings. Such differences do not necessarily imply inconsistent interpretation but rather reflect variable imaging conditions and data quality. Longitudinal lines are frequently uninterpretable over deeply crevassed and thicker ice, where the 25 MHz antenna lacked penetration and thus coherent basal returns (Fig. d). By contrast, cross-glacier profiles are more reliable, benefitting from tie points at rock outcrops along the margins.

The basal interface presents substantial variability in radar expression across the surveyed glaciers. In several profiles, it appears as a transition from low-amplitude, texture-like clutter to a zone of persistently higher backscatter (Fig. a), whereas in others it forms a clearer and more laterally continuous high-amplitude horizon (Fig. c). Some profiles also show strong scattering immediately above the basal reflection, which is nevertheless still clearly recognizable (Fig. b). Bed picking was adapted to the local radar expression and guided by lateral continuity, targeting the deepest laterally coherent basal signal or the onset of persistent enhanced backscatter at the base of the ice thickness. Where no such criterion could be met, no bed pick was assigned. Internal englacial reflectors are generally absent in the 25 MHz data. An exception is the relatively thin Narsaq Bræ (Supplement Fig. S3; location in Fig. a), where profiles show a distinct internal scattering zone at about 20 m depth that is consistent with a cold–temperate ice transition within the glacier (Supplement Fig. S3b).

To assess consistency with existing estimates and place AIRETH picks (referred to as “GPR” here below) into context, we compare bed elevations at crossings with OIB and at collocated points with BM. At the intersections of OIB and GPR, bed elevations mostly follow the 1:1 line (red dots in Fig. a). The median bed difference is about +7 m, which is comparable to our point-wise GPR bed-elevation uncertainty (13 and 22 m for depths of 100 and 400 m, respectively; see Appendix ). A subset of points departs from this pattern, with OIB indicating bed elevations up to about 390 m lower than AIRETH at a few crossings in the Qooqqup Sermia sector. On the contrary, OIB generally yields higher bed elevations than GPR around Sermilik Bræ.

Comparison between GPR and BM bed points show a broad scatter around the 1:1 line (Fig. a; blue dots). Many points lie below the 1:1 line, meaning that AIRETH tends to indicate a lower bed than BM. Moreover, a non-negligible number of AIRETH points are higher than the BM estimate, though. The spread increases with depth and includes spatially coherent clusters deviating in both directions. Overall, the bed difference Δbed=bedGPR-bedBM has a median of −126 m (mean −92 m). A representative profile (Fig. b) illustrates a case where BM is more than 300 m deeper than our interpretation at the deepest point, despite a broadly similar bed shape.

The surface offset Δs=surfGPR-surfBM has a median of −4.9 m, a mean of −2.5 m, and a standard deviation of 21 m, i.e. a few tens of metres at most. These offsets are thus much smaller than the bed differences reported in Appendix , meaning that surface-elevation differences are not the dominant source of the AIRETH–BM mismatch. Rather than attempting a detailed attribution of these discrepancies, we simply note that bedrock elevations from different products can differ by up to a few hundred metres locally, even where surface elevations agree within a few meters.

The above comparisons highlight that helicopter-borne GPR can complement existing products by spatial filling gaps, and by targeting complex marginal terrain and narrow outlet-glacier corridors, at least within the penetration range of the current 25 MHz setup. In our study area, AIRETH and existing products show broadly consistent bed elevations at many locations, although local large mismatches of up to a few hundred meters occur. At the same time, the BM source index indicates that only a small fraction of the BM grid cells are directly constrained by thickness measurements, meaning that local differences should be interpreted with care. In the Sermilik Bræ sector, BM is directly constrained by radar-derived ice-thickness measurements only along a few flight segments (black lines in Fig. a); elsewhere it relies on the inversion between tracks without such data. Similarly, in the northern part of the survey, near Eqalorutsit Kangilliit Sermiat, AIRETH provides additional bed measurements along outlet-glacier trunks where OIB lines are sparse. More generally, we argue that helicopter-borne GPR can supply targeted thickness measurements where outlet glaciers are otherwise unconstrained, particularly in shallower ice conditions. Similarly, such surveys could be applied elsewhere to densify bed observations in regions with sparse or no radar coverage.

Our surveys help to quantify bed-detection performance and practical limitations of the current AIRETH setup. Using a 25 MHz center frequency, bed reflections are generally retrieved up to depths in the order of 300 m (only ∼ 5 % of picks are deeper), whereas attenuation and scattering increasingly mask the bed signal in thicker, crevassed ice, particularly along longitudinal profiles. A lower-frequency configuration (e.g. 12.5 MHz) could extend this depth range, at the expense of vertical resolution. Although higher transmit power could also improve penetration, it is not freely adjustable due to hardware constraints and radio-frequency/aviation regulations. On the positive side, the helicopter platform permits slow flight speeds and tight manoeuvring, enabling dense stacking and targeted coverage in complex glacier geometry. AIRETH can thus be valuable in filling gaps in existing ice thickness products despite its current depth limitation.