Sub-seasonal variability of supraglacial ice cliff melt rates and associated processes from time-lapse photogrammetry
- 1High Mountain Glaciers and Hydrology Group, Swiss Federal Institute, WSL, Birmensdorf, 8903, Switzerland
- 2Institute of Environmental Engineering, ETH Zürich, Zurich, 8092, Switzerland
- 3Key Laboratory of Tibetan Environment Changes and Land Surface Processes, Institute of Tibetan Plateau Research, Chinese Academy of Sciences, Beijing, 100045, China
- 4Geophysical Institute, University of Alaska Fairbanks, Fairbanks, AK 99775, USA
- 5Department of Geography and Environmental Sciences, Northumbria University, Newcastle upon Tyne, NE1 8ST, UK
Correspondence: Marin Kneib (firstname.lastname@example.org)
Melt from supraglacial ice cliffs is an important contributor to the mass loss of debris-covered glaciers. However, ice cliff contribution is difficult to quantify as they are highly dynamic features, and the paucity of observations of melt rates and their variability leads to large modelling uncertainties. We quantify monsoon season melt and 3D evolution of four ice cliffs over two debris-covered glaciers in High Mountain Asia (Langtang Glacier, Nepal, and 24K Glacier, China) at very high resolution using terrestrial photogrammetry applied to imagery captured from time-lapse cameras installed on lateral moraines. We derive weekly flow-corrected digital elevation models (DEMs) of the glacier surface with a maximum vertical bias of ±0.2 m for Langtang Glacier and ±0.05 m for 24K Glacier and use change detection to determine distributed melt rates at the surfaces of the ice cliffs throughout the study period. We compare the measured melt patterns with those derived from a 3D energy balance model to derive the contribution of the main energy fluxes. We find that ice cliff melt varies considerably throughout the melt season, with maximum melt rates of 5 to 8 cm d−1, and their average melt rates are 11–14 (Langtang) and 4.5 (24K) times higher than the surrounding debris-covered ice. Our results highlight the influence of redistributed supraglacial debris on cliff melt. At both sites, ice cliff albedo is influenced by the presence of thin debris at the ice cliff surface, which is largely controlled on 24K Glacier by liquid precipitation events that wash away this debris. Slightly thicker or patchy debris reduces melt by 1–3 cm d−1 at all sites. Ultimately, our observations show a strong spatio-temporal variability in cliff area at each site, which is controlled by supraglacial streams and ponds and englacial cavities that promote debris slope destabilisation and the lateral expansion of the cliffs. These findings highlight the need to better represent processes of debris redistribution in ice cliff models, to in turn improve estimates of ice cliff contribution to glacier melt and the long-term geomorphological evolution of debris-covered glacier surfaces.
Ice cliffs are one of the main contributors to the mass loss of debris-covered glaciers and are likely to contribute to the “debris-cover anomaly”, which describes the tendency of debris-covered glaciers to display similar ablation rates to clean ice glaciers at the same elevation despite the insulating effect of debris (Gardelle et al., 2013; Pellicciotti et al., 2015; Buri et al., 2021). Similar to supraglacial ponds, the surfaces of ice cliffs are directly exposed to energy fluxes from the atmosphere; these cliffs therefore act as “melt hotspots” relative to the surrounding debris-covered ice (Steiner et al., 2015; Buri et al., 2016a; Miles et al., 2016). Indeed, beyond a few centimetres of debris, melt rates reduce exponentially with increasing debris-cover thickness (Ostrem, 1959; Nicholson and Benn, 2006; Reid and Brock, 2010). A series of studies based on high-resolution remote-sensing data acquired from unoccupied aerial vehicles (UAVs) and satellite sensors have shown that ice cliffs enhance melt relative to their surrounding debris-covered area by a factor of 1.2 to 14 (Immerzeel et al., 2014; Juen et al., 2014; Mölg et al., 2019; Thompson et al., 2016; Brun et al., 2018; Mishra et al., 2021; Reid and Brock, 2014) and ponds by a factor of 4 to 8 (Stefaniak et al., 2021; Salerno et al., 2017). Similarly, modelling studies using energy balance models at the scale of an entire glacier or catchment have estimated the melt enhancement factors to be between 6 and 13 for ice cliffs (Buri et al., 2021) and between 9 and 17 for ponds (Miles et al., 2018) for specific locations.
Both remote-sensing and modelling-based approaches to quantify ice cliff melt have limitations. Remote-sensing approaches typically focus on deriving melt estimates from “hotspots” of high thinning identified in maps of elevation change and need to be corrected to account for glacier flow (Vincent et al., 2016; Brun et al., 2018; Miles et al., 2018, 2021; Mishra et al., 2021). However, attributing the melt to the cliffs is non-trivial as they are particularly difficult to map from remote-sensing data, either manually or using automated methods (Herreid and Pellicciotti, 2018; Kneib et al., 2020). Once the cliff outlines at the start and the end of a focus period are known, there are various ways of extrapolating the melt between the two digital elevation models (DEMs) that may lead to varying results (Brun et al., 2016; Mishra et al., 2021), while the cliff outlines may have varied considerably within a few months (Watson et al., 2017b). Wet and cloudy conditions during the monsoon season, when ice cliffs are the most active, present additional challenges for acquiring time series observations of Himalayan debris-covered glaciers using satellite sensors.
The modelling of the cliff energy balance is another way to tackle the problem of the cliff contribution to glacier melt. It has evolved in the past 2 decades from the point scale (Sakai et al., 2002; Han et al., 2010; Reid and Brock, 2014; Steiner et al., 2015) to a distributed representation of the energy balance at the cliff surface (Buri et al., 2016a). Accounting for the cliff energy balance to dynamically update the cliff geometry (Buri et al., 2016b) has led to a better understanding of the controls of ice cliff evolution, including aspect (Buri and Pellicciotti, 2018), and to the estimation of ice cliff melt contribution at the catchment scale (Buri et al., 2021). This complex modelling framework is, however, still limited in the representation of the interaction of ice cliffs with their surroundings. For example, the model presented by Buri et al. (2016b) accounts for debris redistribution by removing debris on slopes solely based on a fixed slope threshold and, for ice cliffs which are attached to a pond, uses a fixed value of pond melt at the cliff base. Moreover, the model parameters have only been evaluated using a small sample of cliffs, where data have been collected over short timescales using ablation stakes, by measuring the backwasting rate of the cliff edge (Sakai et al., 1998, 2002; Han et al., 2010; Reid and Brock, 2014; Steiner et al., 2015; Buri et al., 2016a) and, more recently, using measured volume changes (Buri et al., 2016b). Ultimately, fully distributed energy balance models require knowledge of meteorological and surface variables over the cliff's surface and the surrounding debris slopes, such as albedo, which are difficult to determine and which vary much in time and space.
These limitations highlight the need for detailed and quantitative observations of cliff melt and evolution during the melt season. This is particularly challenging as ice cliffs are dynamic features which can grow, shrink, appear or disappear within the course of a single season (Sato et al., 2021; Kneib et al., 2021), which results in the ice cliff area regularly changing by up to 20 % from year to year (Kneib et al., 2021; Watson et al., 2017a; Steiner et al., 2019; Falaschi et al., 2021; Sato et al., 2021; Anderson et al., 2021). This high variability can be explained by the strong influence of local processes such as pond undercutting, filling and drainage (Kraaijenbrink et al., 2016; Watson et al., 2017b), stream undercutting (Mölg et al., 2020), and debris redistribution (Moore, 2018; Westoby et al., 2020). To improve process understanding and, in turn, inform the refinement of numerical models, observations of ice cliff evolution therefore need to (1) be captured during the melt season, when ice cliff activity is at its highest; (2) be of high spatio-temporal resolution; and, in turn, (3) be suitable for quantifying surface changes both across ice cliffs and on adjacent local topography and features, including debris-covered ice, and supraglacial streams and ponds.
In the past decade, advances in modern structure-form-motion photogrammetry have enabled the reconstruction of 3D topography from images acquired from multiple, converging viewing angles (Westoby et al., 2012). A primary use of SFM-based approaches has been to map glacier surfaces from UAVs, enabling the detailed study of debris-covered glaciers and their supraglacial features (Immerzeel et al., 2014; Kraaijenbrink et al., 2016; Brun et al., 2018; Westoby et al., 2020; Mishra et al., 2021). Topographic reconstruction can also be achieved through terrestrial photogrammetric survey, which can enable the accurate mapping of steep and overhanging features which are common at ice cliff locations (Brun et al., 2016; Watson et al., 2017b; King et al., 2020) and can be occluded in imagery acquired from nadir-oriented aerial surveys. The combination of high-frequency time-lapse image capture and photogrammetric processing is therefore highly promising for generating quantitative observations of the dynamics of fast-changing cryospheric landscapes. While still limited by the amount of processing required and the logistical aspects of deploying arrays of time-lapse cameras, time-lapse photogrammetry has been used successfully to precisely monitor thaw slump activity (Armstrong et al., 2018), lava flows (James and Robson, 2014b), snowmelt (Filhol et al., 2019) and calving dynamics (Mallalieu et al., 2017).
Here we apply time-lapse SFM photogrammetry to study the sub-seasonal melt of four ice cliffs on two different glaciers of the Himalayan range, at weekly intervals during a full melt season. We aim to quantify ice cliff sub-seasonal melt and identify the local processes controlling its variability. To this end, we derive weekly flow-corrected DEMs of the ice cliffs and calculate spatially distributed melt over the study period. We compare these results with estimates of melt generated by a 3D energy balance model to isolate the main energy fluxes and identify the local processes that cause modelled melt to deviate from our measurements.
2.1 Study sites
We installed time-lapse camera arrays on two Himalayan debris-covered glaciers with distinct glaciological and climatic characteristics (Fig. 1). Langtang Glacier is located in central Nepal (85.72∘ E, 28.27∘ N) and has a 15 km long debris-covered tongue, with an estimated density of supraglacial ice cliffs (ponds) ranging between 2.1 % and 4.7 % (0.9 % and 2.5 %) of the debris-covered area (Kneib et al., 2020, 2021; Steiner et al., 2019; Miles et al., 2017b). The debris thickness increases down-glacier and exceeds 2 m in the lower portion of the glacier (McCarthy et al., 2022), where our survey domain was located (Fig. 1c). 24K Glacier (hereafter “24K”) is located in eastern Tibet (95.72∘ E, 29.76∘ N), is also extensively debris-covered but is much smaller than Langtang Glacier; it has a 2 km long debris-covered tongue, and debris-cover is thinner (at most 0.5 m in the lower portion of the glacier) (Fig. 1d). The debris-covered area of 24K is much steeper (9.8∘) than for Langtang (3.4∘), which may partly explain the scarcity of ponds at its surface and the presence of a number of supraglacial streams in its central area which have led to the development of so-called “cryo-valleys” bounded by ice cliffs, and similar to those described on Zmutt glacier in Switzerland (Mölg et al., 2020).
We installed an array of eight time-lapse cameras on the lateral moraine of Langtang Glacier, overlooking a small domain of the lower portion of the debris-covered tongue and comprising a number of north-east- to north-west-facing ice cliffs, three of which are connected to a pond (Fig. 1a). An additional array of four time-lapse cameras was installed on 24K, overlooking a large stream-influenced north-facing cliff (Fig. 1b).
2.2 Time-lapse camera arrays
The time-lapse cameras were mounted directly on stable boulders along lateral moraine crests of the two glaciers (Fig. 1a, b). The custom time-lapse rigs consisted of a Canon EOS 2000D camera (24.1 MP) with an 18–25 mm lens. The cameras took photographs at a consistent 2 h interval for the whole duration of the melt season, triggered by an intervalometer. The cameras were powered by a 5 W solar panel, a 12 V 7 A h lead–acid battery and an ECO-N-T solar charge controller (Fig. 2a). These elements were assembled in a weatherproof box (BixiBox) which was mounted on a 1.5 m long aluminium mast bolted vertically to the rock (Fig. 2b, c). All camera stations ran without data gaps from 12 May to 1 November 2019 (6 months) for Langtang and from 8 June to 12 October 2019 (4.1 months) for 24K. The focal length of all cameras was manually set to 18 mm to ensure the widest viewing angle. The xyz position of each time-lapse camera was measured using a differential GPS (dGPS), and the three viewing angles were measured at the beginning and at the end of the time-lapse period.
2.3 UAV flights and remote-sensing imagery
We carried out a UAV survey of the study domain at the start and the end of the monitoring period on 24K. On Langtang, a flight was only possible at the end of the study period (Table 1). The initial and final conditions for Langtang were instead constrained with two Pléiades satellite stereo images taken within a month of the start and the end of the time-lapse recording period (Table 1).
The UAV images were taken nadir-oriented at a fixed elevation of 70 to 120 m above the glacier surface with a lateral overlap of 70 % and a forward overlap of ≥ 80 %. Additional oblique images of the survey domain, which have been proven to mitigate against the introduction of systematic model deformation (James and Robson, 2014a), were taken manually, depending upon UAV battery limits.
Between 15 and 18 ground control points (GCPs) were laid out across the survey domain around the main features of interest (ice cliffs, ponds and streams), with a good distribution between topographic lows and highs (Fig. 4) and consistent coverage at margins of the study area. GCPs were visible in photographs captured by the time-lapse cameras and from the UAV. The xyz positions of the GCPs were measured with a single-band dGPS system (10 cm accuracy) within 48 h of the UAV flights.
2.4 GPR measurements
We conducted ice thickness measurements using a Kentech ground-penetrating radar (GPR) monopulse generator with 20 m dipole antennas (∼ 2.5 MHz) along four transects on 24K Glacier in October 2019 (Fig. 1b). For Langtang, we used the measurements from Pritchard et al. (2020) conducted in the vicinity of the survey domain (Fig. 1a). These measured ice thicknesses were used to bias-correct the consensus ice thicknesses from Farinotti et al. (2019) using a linear regression of the ice thickness for Langtang and of the bed altitude for 24K to obtain a distributed estimate of ice thickness for each survey area. These corrections led to the reduction of the mean bias from 15.8 to 0.1 m and from 94.1 to 1.7 m for Langtang and 24K, respectively.
2.5 Field observations of supraglacial ponds
Two of the cliffs in the Langtang survey domain had a pond at their base in May 2019, at the start of the recording period. We monitored the two pond water level changes using HOBO pressure transducers and recorded the water surface temperature using a HOBO thermistor attached to a float. The pond at the base of one cliff drained almost entirely during the study period, and it was not possible to retrieve its pressure transducer, which got buried by a thick layer of debris. The thermistor was, however, still accessible, and its temperature record combined with the observations from the time-lapse cameras clearly shows the timing of the drainage.
2.6 Meteorological observations
Each glacier was equipped with an on-glacier automatic weather station (AWS), which was installed in the vicinity of the survey domain (< 100 m of elevation difference) and recorded, among other variables, air temperature, relative humidity, incoming and outgoing longwave and shortwave radiation, and wind speed at 5 min intervals over the study period (Fugger et al., 2022). Precipitation measurements were acquired using a HOBO tipping bucket at the AWS site for 24K and on the lateral moraine, ∼ 500 m away from the AWS, for Langtang (Steiner et al., 2021). The air temperature measured at the AWS location was lapsed considering the mean above-debris lapse rates (−0.0088∘ C m−1) following Shaw et al. (2016). All other variables were left unadjusted for input to the energy balance model (Sect. 5.7).
3.1 Processing of UAV and Pléiades images
The Langtang Pléiades satellite images were stereo-processed to generate 2 m resolution DEMs and 0.5 m resolution orthoimages from the panchromatic band using rational polynomial coefficients (RPCs) within the NASA AMES Stereo Pipeline (Kneib et al., 2020; Beyer et al., 2018; Shean et al., 2016).
The Langtang and 24K UAV images were imported to Agisoft Metashape Professional (v1.7.2). Initial bundle adjustment was performed using only the UAV GPS geotags. We then incorporated the xyz positions of the GCPs to refine this adjustment and improve camera location and pose estimation and the location of image tie points (Westoby et al., 2020). We then generated dense point clouds, which were used to produce DEMs and orthoimages (0.2 m resolution for the Langtang survey, 0.12 m for the 24K survey).
Co-registration of the Langtang Pléiades DEMs was performed over off-glacier stable terrain with slopes between 10 and 45∘, following the approach detailed in Nuth and Kääb (2011). For the 24K UAV flights, we used the fixed position of the time-lapse cameras, which we measured during each dGPS survey, to correct for vertical and horizontal shifts in the position of the on-glacier GCPs. After the initial co-registration of the UAV DEMs, there remained some non-linear distortions (tilts) that were removed using additional natural off-glacier control points (boulders) on both sides of the glacier identified in the June flight to rerun the bundle adjustment of the October flight, which improved the co-registration (Sect. 3.3).
For both sites, we estimated the vertical uncertainty as the standard deviation of the DEM difference over off-glacier stable terrain (Mishra et al., 2021), 0.53 m for Langtang and 0.50 m for 24K.
3.2 DEM processing with time-lapse photogrammetry
The overall workflow for generating DEMs from the time-lapse images broadly follows that described by Mallalieu et al. (2017) (Fig. 3). The time-lapse lasted from 12 May to 1 November 2019 (173 d) for Langtang and from 8 June to 12 October 2019 (126 d) for 24K, resulting in ∼ 2100 images per camera for Langtang and ∼ 1550 images per camera for 24K, at 24.1 MP resolution.
In the first step (step 1, Fig. 3) we manually removed all the images taken during night time, with water or snow in front of the lens or with poor visibility due to clouds or precipitation. We then grouped the images from the different cameras taken at each site within 2.5 h periods to account for offsets in the image acquisition time of the different cameras. If one or more images were missing, we ignored all the images in that set. After this pre-selection, there remained 781 image sets for Langtang and 357 for 24K.
We used the image sets of 1 November 2019 14:00 for Langtang and 8 June 2019 14:00 for 24K as “reference” sets, as they were taken within a few hours of the GCP surveys conducted in the survey domain (Fig. 4). In step 2, the reference image sets were imported to Agisoft Metashape Professional (v1.7.2), and we used the dGPS-measured position and viewing angles of the cameras in the initial bundle adjustment and then used the GCP coordinates for subsequent optimisation of the lens parameters prior to generation of the dense point cloud (Fig. 3). These reference sets were used to define “pseudo” GCPs (PGCPs), which, combined with their camera parameters, were used to process the weekly images sets (step 3; Sect. S1 in the Supplement; Figs. 3, 4).
We established the relative accuracy of the output DEMs by computing the mean and standard deviation values of elevation change relative to the reference DEM calculated over background stable terrain (Fig. 4, orange outline). The mean elevation change over this area of the background moraine was generally < 0.2 m for Langtang and < 0.05 m for 24K. Higher values were obtained when the illumination conditions in a given image set differed substantially from the reference image set, or when some of the images were slightly blurred from rain or mist. In these instances, we used other, higher quality image sets taken within a few days from the target date.
Ultimately, we produced 25 time-lapse DEMs and orthoimages for Langtang (0.20 m resolution) and 19 DEMs and orthoimages for 24K (0.24 m resolution), covering the full study period at an approximately weekly interval (Table S3).
We used the orthoimages to manually delineate the ice cliff outlines at each weekly time step, which we considered to be the exposed ice sections free of debris. This was sometimes difficult in the case of patchy debris, which was included in the cliff outlines when the underlying ice was still visible. Oblique viewing angles combined with a complex glacier surface led to gaps in the orthoimages and DEMs caused by topographic shadowing. Despite this limitation, we still resolved the larger portion of three cliffs on Langtang and of the 24K cliff (Fig. 4a, b).
3.3 Glacier flow corrections
In a fourth step (step 4, Fig. 3), all the DEMs, except a reference DEM, for each glacier were corrected to account for glacier flow (horizontal surface velocity and emergence) following the approach described by Mishra et al. (2021), using estimates of distributed surface velocity and ice thickness to calculate the ice flux through a flux gate and, in turn, an implied ice emergence velocity. We calculated distributed surface velocity fields over the lower portion of the glaciers, including the survey domains, by applying a normalised cross-correlation approach to the Pléiades (for Langtang) and UAV (for 24K) DEM hillshades using ImGRAFT (Messerli and Grinsted, 2015). We filtered these velocity fields by removing values with a low signal-to-noise ratio (< 2), low correlation score (< 0.5) or unrealistically high values (> 3 m for Langtang, > 8 m for 24K over the study period) and interpolated the remaining results with a cubic spline interpolation (Mishra et al., 2021).
We used these velocity fields to correct the x-y displacements between the different DEMs (time-lapse, UAV, Pléiades) and the reference time-lapse DEMs, assuming a constant velocity over the study period. In this step, we also accounted for vertical displacement due to the downslope advection of the surface using the slope from the AW3D 30 m resolution DEM (Tadono et al., 2014) of each study area, smoothed using a 30-pixel Gaussian filter (Mishra et al., 2021; Miles et al., 2018; Brun et al., 2018).
We calculated emergence velocity in the lower portion of the glaciers (including the survey domains) by estimating the flux through a flux gate located immediately upstream from the survey domains, taking into account the surface velocity and the adjusted ice thickness at this location (Mishra et al., 2021; Miles et al., 2018; Brun et al., 2018; Vincent et al., 2016) at a resolution of 8 m for Langtang, 4 m and for 24K, assuming that basal sliding accounts for 50 % of the surface motion (but considered the full 0 %–100 % range in the uncertainty calculation). We integrated the flux across the cross-section with a simple-shear assumption to calculate the column-averaged velocity (Huss et al., 2007) and assumed that this flux is uniformly distributed as emergence downstream from the flux gate.
We estimated the surface velocity uncertainty as the normalised median absolute deviation of its x and y components over off-glacier terrain, equal to 0.84 m (0.6 cm d−1) for Langtang and 0.35 m (0.3 cm d−1) for 24K over the full study period. We obtained an emergence velocity of 0.39 ± 0.16 m (0.3 ± 0.1 cm d−1) for Langtang and 0.66 ± 0.16 m (0.5 ± 0.1 cm d−1) for 24K. As for the x-y displacements, we used these emergence values to correct the different DEMs (time-lapse, UAV, Pléiades) relative to the reference time-lapse DEMs, assuming a constant emergence over time. Similarly to the DEMs, the cliff outlines were flow-corrected for the surface displacements in the x and y directions.
3.4 Estimating melt from DEM differencing
In this study, we were interested in calculating distributed melt patterns at the surface of the cliffs, which correspond to the normal displacement of the cliff surface (Buri et al., 2016b). A number of studies used the M3C2 algorithm (Lague et al., 2013; Watson et al., 2017b; Mishra et al., 2021) directly applied to the point clouds to calculate this normal displacement. However, here we aimed to compare our results with a gridded ice cliff energy balance model (Buri et al., 2016a, b), which uses the cliff DEM for the distributed energy balance calculations. We therefore estimated the melt from two time-lapse DEMs (DEM1 and DEM2) by calculating for each pixel of DEM1 the local normal based on its eight neighbouring pixels and finding the intersection of the normal with DEM2. The melt was then equal to the distance between the DEMs along this normal (Fig. S1 in the Supplement). This approach is similar to the M3C2 algorithm but using DEMs and 3×3 neighbourhoods.
3.5 Uncertainty estimation
To estimate the uncertainty in melt rate, we combined the uncertainties from the flow correction σflow with an estimation of the uncertainty of the calculation of melt distance from the DEM's σDEM.
We conservatively assumed the melt distance uncertainty σDEM to be equal to the uncertainty in elevation change as this removes the dependence on the terrain aspect and slope. Indeed, in the case of two DEMs with the same slope parallel to one another, which we considered to be the most common short-term change due to ice melt, the elevation difference should be larger than the melt distances (e.g. Mishra et al., 2021), and the same should be true for their uncertainties. In the case of our study areas with complex geometries and viewing angles, we expected these uncertainties to vary with slope and aspect, as well as with the number of overlapping images, the distance from the time-lapse cameras and the time difference with the reference DEMs (James and Robson, 2014b; Mallalieu et al., 2017; Armstrong et al., 2018; Filhol et al., 2019). We also expected elevation change uncertainties to increase with time from the reference image set and distance from the time-lapse cameras, except in the very near field where less overlap of the images should lead to higher uncertainties (Mallalieu et al., 2017).
The uncertainty from the melt distance's σDEM comprises a systematic error σDEM,sys given by the absolute mean elevation change over stable terrain and a random error σDEM,rand given by the standard deviation of elevation change over stable terrain. Depending on the evolution of the uncertainties in space, this relationship can be scaled by a factor f:
We therefore estimated the melt uncertainties in the cliff domain by analysing the mean and standard deviation of elevation change over the moraine (Fig. 4). Indeed, the moraine was the closest feature to the survey domain that could be considered relatively “stable”, at least over a period of a few months. Furthermore, it had similar slopes and aspects to those of the cliffs in the survey domain but was located in the background of the survey area, making it a good but conservative proxy for the features analysed (Fig. 4). We conducted two different tests to estimate the melt uncertainties in the cliff domain. The first test (1) was to look at the evolution of the mean and standard deviation of the elevation changes relative to the reference DEMs over the moraine with time (Fig. 5a, b). The second test (2) was to look at the evolution of the mean and standard deviation of the elevation changes with distance for time-lapse DEMs taken within a few days from each other (Fig. 5c, d).
The mean value remained between ±0.2 m for Langtang, where the moraine was ∼ 800 m away from the cameras (Fig. 5a), and between ±0.05 m for 24K, where the moraine was ∼ 400 m away from the cameras (Fig. 5b). Using a factor of 2 to account for positive and negative biases, we obtained m for Langtang and m for 24K (Table 2). σDEM,rand, given by the standard deviation, increased with time during the first 2 months of the time series for Langtang until it reached a value of ∼ 1 m, while it remained stable around 0.6 m for 24K during the whole period. For (2), we took the DEM the furthest away in time from the reference DEM and processed the image pairs taken within 48 h of this new reference DEM, only keeping the resulting DEMs with a mean elevation change relative to the reference DEM lower than 0.2 m for Langtang (four remaining DEMs) and 0.05 m for 24K (seven remaining DEMs) (Fig. 5a, b, dashed lines). The elevation change patterns of these near-contemporaneous DEMs highlighted a factor f=2 increase in standard deviation with distance between the cliff domain and the moraine for Langtang and f=1.7 for 24K (Fig. 5c, d). As a result, for Langtang σDEM=0.5 m and for 24K σDEM=0.4 m (Table 2). These are the same values as if we had calculated them from the random errors only, which means that the systematic errors can be considered negligible.
We also needed to account for the uncertainties related to the flow correction, which we assumed to be equal to the quadratic sum of the 1σ surface velocity uncertainty σxy; the 1σ emergence velocity uncertainty σb estimated following the approach and assumptions described by Miles et al. (2018); and the uncertainty from the slope correction σSlope (all in m d−1):
where α is the mean glacier slope in the survey domain and us the mean velocity. For the uncertainty on the slope correction, we assumed a rad uncertainty in the slope angle, which results in σSlope=0.03 cm d−1 for Langtang and 0.06 cm d−1 for 24K. As a result, the 1σ uncertainty from flow correction was equal to 0.007 m d−1 for Langtang and 0.004 m d−1 for 24K.
The 1σ melt uncertainty for each pixel could be expressed as
where dt is the number of days over which the melt is calculated. Ultimately, we calculated melt on a tri-weekly basis for Langtang and a bi-weekly basis for 24K to reduce the uncertainties relative to the measured melt rates. This meant that the uncertainty from flow was an order of magnitude lower for these domains and could therefore be neglected: m (0.02 m d−1) for Langtang and m (0.03 m d−1) for 24K over their respective tri- and bi-weekly melt periods (Table 2).
Based on this, in all that follows we used the standard deviation of melt at the cliff location to represent these uncertainties, as it directly accounts for (1) the random error from the DEMs and (2) the melt variability at the surface of the cliffs. We note, however, that assuming a Gaussian error for independent measurements, the random error from the DEMs becomes negligible (< 0.05 m) for the average melt when the number of pixels considered is greater than 100, which is always the case here.
3.6 Cliff brightness and snow events
For 24K, we found the brightness of the cliffs to change substantially with time. We estimated this brightness for each set of images (781 for Langtang, 357 for 24K), by taking the average value of the blue band in a 200×100 pixel domain at the centre of cliff 1 (Langtang) and of the main 24K ice cliff (Fig. S2). We normalised this brightness value by the mean value of the blue band in a domain of the same size over a debris-covered slope with similar slope and aspect characteristics, giving a basic proxy for apparent changes in ice cliff albedo insensitive to illumination differences between scenes. We used the blue band as when comparing the visible spectra of cliffs and debris of different brightnesses, this was the band that highlighted the strongest differences. We took a single brightness value for all cliffs with different slopes and aspects in the domain, as the brightness appeared to evolve in a similar way across all cliffs (Fig. S2).
We additionally looked at the daily influence of snow events on ice cliff melt at both sites. We considered that there was a snow event (1) when the daytime shortwave albedo at the AWS location was higher than 0.3 or (2) when snowfall or fresh snow cover on the glacier could be observed in at least one of the time-lapse images on a given day.
3.7 Energy balance model
We compared our tri- to bi-weekly melt patterns with the melt obtained over the same period using a static cliff energy balance model (Buri et al., 2016a). The model calculates the energy inputs from shortwave, longwave and turbulent fluxes in a distributed way across the cliff surface. The static version of the model that we used has been described extensively in the past literature, which we invite the reader to refer to for further details (Steiner et al., 2015; Buri et al., 2016a). We used the exact same parameters as Buri et al. (2016a) at both sites and did not conduct any further calibration.
The model was run over the exact same periods over which we calculated melt from DEM differencing, without simulating surface geometry changes. We used the static version of the model to focus on the contribution of the different energy-fluxes only, thus removing the influence of the modelled geometry updates. Indeed, the cliff dynamic model was designed to represent changes over long periods (entire melt season or monthly intervals), for which the melt rates are high relative to the model's spatial resolution. Due to the limited data available for the model development, the processes influencing the cliff dynamics (debris redistribution, additional melt from ponds) were also represented by rather simple parameterisations lumping together distinct physical processes. While this dynamic model is appropriate to estimate bulk changes over long periods (Buri et al., 2021; Buri and Pellicciotti, 2018; Buri et al., 2016b), we considered it to be too simple to represent all the complexity of changes occurring on a weekly timescale and therefore less reliable to understand the local energy balance.
We used the gap-filled time-lapse DEMs as the reference surface over which to calculate the energy fluxes and the debris viewing angles and near-field horizon calculations. We filled the gaps using the UAV DEMs corrected with the elevation change signal from the Pléiades (for Langtang) and UAV (for 24K) DEMs. To reduce computation time, the DEMs were resampled to 0.6 m. We used the 30 m AW3D DEMs (Tadono et al., 2014) of the area for the far-field horizon calculations and did not include debris redistribution or additional melt from the ponds.
We used data from the nearby on-glacier AWSs as meteorological forcing for the ice cliff model and estimated debris surface temperature, which is an additional model input, from the outgoing longwave radiation at those AWSs. Importantly, we assumed a fixed albedo of 0.15 for debris and 0.2 for ice, which were the same values used in the original studies, calibrated on Lirung glacier, which is located in the vicinity of Langtang Glacier (Steiner et al., 2015; Buri et al., 2016a).
4.1 General measured and modelled melt patterns
4.1.1 Site-scale melt patterns
Elevation change patterns between the pre- and post-monsoon period from the UAV and Pléiades DEMs alike showed enhanced surface lowering at the location of the ice cliffs (Fig. 6a, b). Elevation change patterns displayed some variability in the non-cliff area of the domain, and this was especially visible with the higher-resolution data from 24K (Fig. 6b). Sub-debris melt on 24K, where the debris-cover was thinner (Fig. 1; McCarthy et al., 2022), also appeared to be higher than on Langtang (Fig. 6b). In both domains, cliff backwasting is evident (Fig. 6a, b), varying from cliff to cliff and site to site, between 0 and 5 cm d−1 on Langtang and 4 and 9 cm d−1 on 24K. There were also signs of cliff expansion (e.g. cliff 3 on Langtang) and reburial (e.g. 24K main cliff). The mean and standard deviation of the sub-debris melt calculated from the flow-corrected Pléiades and UAV DEMs and for snow- and cliff-free (including a 5 m buffer around the initial and final cliff outlines) zones were −0.3 ± 0.4 cm d−1 for Langtang and −1.1 ± 0.5 cm d−1 for 24K, 11–14 (4.5, respectively) times less than the average cliff melt measured from the time-lapse DEMs (Fig. 6).
The high temporal resolution of this dataset enables one to precisely estimate the total and spatially-averaged melt of ice cliffs, while the estimates from the Pléiades and UAV DEMs are usually 5 % to 80 % off depending on the method used to extract these values (Tables S4, S5), due to the mixing of ice cliff and sub-debris melt contributions for less temporally resolved data.
To disentangle the different components of the ice cliffs' evolution, we focused the analysis of the sub-seasonal patterns on six transects of the three main Langtang cliffs and four transects of the 24K cliff, which kept similar aspect and slope during the whole study period (Fig. 6a, b) and were all west to north-east facing. The mean measured and modelled melt were comparable for each of those transects, with ≤ 25 % difference and no consistent bias, even though there was a higher variability in measured melt (Fig. 6c). The observed daily cliff melt was in general higher (3.9–5.1 cm d−1) for 24K than for Langtang (2.9–4.3 cm d−1). At the seasonal scale, there did not appear to be a control of slope or aspect on melt (Figs. 6c, S3).
4.1.2 Melt patterns as a function of time
The time-lapse observations at both sites started a few days after the ice cliffs became snow-free and ended after the first snowfalls. Overall, air temperatures were higher at 24K by 4–5 ∘C, but this difference was partly compensated by higher incoming shortwave radiation on Langtang (Fig. 7c and d). The incoming longwave radiations was of a similar value, and plateaued during the whole monsoon season. Melt patterns at the two sites differed considerably. Melt was higher at the start of the study period (pre-monsoon; 3.4 ± 1.5 cm d−1 for Langtang, 6.7 ± 2.1 cm d−1 for 24K) than at the end (post-monsoon; 0.7 ± 1.1 cm d−1 for Langtang, 1.1 ± 1.0 cm d−1 for 24K) (Fig. 7) and exhibited similar variability over the study period at both sites (coefficient of variation of 0.37 for Langtang cliff 3 and 0.34 for the 24K cliff). The peak in melt was reached in the last week of June and first week of July on Langtang (6.4 ± 1.9 cm d−1) and around mid-August on 24K (7.3 ± 1.8 cm d−1). This peak in melt on Langtang corresponded with the timing of the peak in air temperature, but while air temperature stabilised between early July and early September, melt started to decrease from early July, coinciding with the decrease in incoming shortwave radiation and increase in longwave radiation at the start of the monsoon period (Fig. 7c). The peak in melt at 24K also corresponded to the maximum air temperature, but similar to Langtang, the incoming shortwave radiation had a direct influence on this melt pattern (Fig. 7d). The observed melt behaviours were well represented by the modelled melt but with slightly smaller amplitudes.
4.2 Processes occurring at each cliff
For the detailed analysis of the melt patterns of Langtang cliffs 2 and 3 and the 24K cliff, we used transects perpendicular to the cliff outlines to derive average values across different vertical sections of the cliffs (Figs. 10–14).
4.2.1 Langtang cliff 1
Langtang cliff 1 was a relatively small (5–10 m tall, 30–40 m wide), north-facing cliff (Figs. 8, 9). In July, it expanded a few metres to the east, resulting in enhanced melt rates at this location, but the new section got re-buried relatively quickly in August. Indeed, the small cavity at the base of the cliff (visible at the start of the study period, Fig. 8a) increased in size as the cliff backwasted, debris falling from the top of the cliff accumulated in the cavity slowly reburying this section of the cliff, which by the end of the period, had become very shallow (Fig. 8f). The measured melt displayed a similar signal to that of Langtang cliff 3 (Fig. 7a, 8f) and was relatively homogeneous across the cliff surface, except for higher values at the location of the cliff expansion (Fig. 8h). The large boulder standing on top of the cliff did not seem to influence the melt (Fig. 8d–f). The modelled fluxes showed a strong contribution of shortwave radiation to the cliff energy balance, with an increase in the contribution of net turbulent fluxes from 9 % to 36 % between the end of May and mid-July when the net shortwave decreased by 38 % with the arrival of the monsoon (Fig. 9d). The net longwave radiation contributed negatively to the cliff's energy balance.
4.2.2 Langtang cliff 2
Langtang cliff 2 was a medium size (10–20 m tall, 35–45 m wide), west-facing cliff that was attached to a pond at the start of the study period (Figs. 10, 11) and displayed higher melt rates than at cliff 1. The time-lapse images showed that the pond partly drained between 2 and 5 July. This was confirmed by the pond surface temperature data (Fig. 11c), which showed much stronger temperature variations after the end of June, proof that the sensor had become grounded on the debris. The vertical step left by the pond at the cliff base after draining got progressively reburied and had disappeared by mid-August (Fig. 10c, d). The cliff had a concave shape at the start of the study period, being steeper at the top than at the bottom. At the end of June, triggered by the cliff backwasting, part of the debris-covered slope above the cliff slumped, thus expanding the cliff upwards, at a lower angle (Figs. 10, S6). This upper debris-free area expanded laterally in July, enhancing the sharp transition between the lower steeper portion that was progressively reburied after the drainage of the pond and the upper shallower portion of the cliff that became predominant with time. This reburial of the lower steeper section and expansion of the upper shallower section led to the cliff doubling in size in July and then returned to its initial size by early September.
In parallel, melt increased from 3.0 ± 0.7 (3.2 ± 1.0) cm d−1 at the end of May to more than double – 6.8 ± 1.7 (6.5 ± 0.8) cm d−1 – at the end of July for transect 1 (transect 2). These values were substantially higher than the melt predicted by the energy balance model and mostly due to the higher measured melt on the upper, shallower section of the cliff (Fig. S5). However, for both transects there was a sharp reduction in melt synchronous with the progressive reburial of the cliff (Fig. 11). Melt then plateaued around 2.7 ± 2.7 cm d−1 for transect 1 and 3.3 ± 1.3 cm d−1 for transect 2 and finally decreased to almost null values in October.
4.2.3 Langtang cliff 3
Langtang cliff 3 was a relatively large cliff (20–30 m tall, 70–100 m wide) which was predominantly north-east facing at the start of the period but expanded to north-facing slopes during the study period (Fig. 12). There was a large pond at the base of the cliff for the whole study period which persisted throughout the season but also slowly drained by a total of 1.7 m (Fig. 13c), leaving a notch at the base (Fig. 12a–f). Most of the drainage occurred in July. The north-facing debris-covered slope to the east of the cliff steepened in June and July and started slumping at the end of July, when the notch appeared under the debris, revealing that the pond had also been undercutting this slope. The slumping accelerated and the slope was mostly debris-free by the end of August, leading to a doubling of the cliff area between the end of July and the end of September (Fig. 13b). Despite a decrease in shortwave radiation at the end of August for transect 1, melt increased in August synchronously with a reduction in slope linked with the slumping of the north-facing slope (Fig. S8). Most of the backwasting occurred at the shallower section of the cliff that was disconnected from the pond until the end of July, while the steeper (50–65∘) section of the cliff in contact with the pond displayed lower backwasting rates.
4.2.4 24K cliff
On 24K, we focused on a set of linked cliffs at the centre of the survey domain, 130 m wide and 10–20 m tall (Figs. 14, 15). These cliffs, which could also be regarded as one single cliff split by patches of thin debris, occupied the slopes of the outer bend of a supraglacial stream which was flowing directly at the base of the ice cliffs, sometimes undercutting the ice slopes. The centre of the bend was steeper and was occupied by a large continuous cliff, while the sides displayed a changing combination of debris patches and bare ice (Fig. 14). This configuration remained throughout the study period except on the west side of the meander (transect 1), where the stream disconnected from the ice cliff during the study period (Fig. 15a), causing a progressive reburial of this outer section in July and August (Fig. 14). This was just a small portion of the cliff, and overall the cliff area did not change by more than 10 % over the whole study period; and the aspect and slope of the different transects remained consistent (Fig. S10).
The different transects displayed comparable temporal melt and energy balance patterns (Fig. 7), with an increase from June to the mid-August peak followed by a steeper decrease until the end of the study period in early October, characterised by close to zero melt values and regular snowfalls (Fig. 7b). The melt variability was driven by net shortwave radiation, which also represented more than 50 % of the energy budget during the whole study period. Contrary to Langtang, the net longwave contributed positively to the cliff energy balance due to higher air temperatures and therefore higher incoming longwave from the atmosphere (Fig. 7). Transects 1, 3 and 4 displayed high (7–8 cm d−1) melt values at the very start of the study period, which were not represented by the energy balance model. These high values exceeding modelled melt at the start and at peak melt, as well as the general patterns throughout the season, also followed an inverse pattern with cliff brightness (Fig. 15c), which was itself correlated with precipitation (Fig. 15b). Transects 2 and 4 were the ones where measured and modelled melt disagreed the most (up to 25 % difference), with generally lower measured melt rates than predicted by the model, and also the ones with the most patchy debris, where outlining the cliff extents was particularly difficult.
The sub-seasonal observations of ice cliff melt, evolution and the underlying processes were made possible thanks to the use of time-lapse photogrammetry, which enabled the semi-automated production of weekly DEMs of the survey area with an estimated uncertainty of ±20 cm (±6 cm) for Langtang (24K). This is a novel approach, the advantages and drawbacks of which we discuss in detail in the Supplement Sect. S2 (use of time-lapse photogrammetry approach). Here we discuss instead the main findings that the new setup allowed, in terms of understanding cliff melt rates and contribution to mass losses (Sect. 7.1), as well as the processes that control their evolution and are not yet included in current models (Sect. 7.2). The different mechanisms outlined here are indicated in Fig. 16, which represents one possible evolution pathway for a set of idealised cliffs.
5.1 Controls on ice cliff melt variability
The studied cliffs displayed melt rates at 4.5 times higher than the surrounding debris-covered ice on 24K and 11–14 times higher on Langtang, where thick debris (> 0.5 m) in the lower portion of the glacier prevents almost any sub-debris melt (Miles et al., 2021; McCarthy et al., 2022), thus promoting the melt-generating role of cliffs. While the cliff melt values are comparable to previous estimates for other debris-covered glaciers based on cliff volume loss and backwasting rates (e.g. Sakai et al., 1998; Juen et al., 2014; Brun et al., 2016; Mishra et al., 2021), the high-temporal-resolution estimates are more accurate, as they allow calculations of melt over strongly varying cliff geometries. Changes in cliff melt rates over time from the time-lapse DEMs ranged between 0 and 8 cm d−1 and captured the progressive changes in cliff area and shape (Figs. 8–15), thus enabling a new, more precise estimate of cliff melt compared to the values extracted from the beginning- and end-of-season DEMs (Pléiades and UAV DEMs) (Table S4). This is the first time that the sub-seasonal variability of ice cliff melt has been quantified, and it shows that use of only beginning- and end-of-season cliffs' geometries, neglecting the history of area and geometry changes over a melt season, can lead to an underestimation of about 50 % in melt rates (Table S4).
Exchange of energy with the atmosphere controlled cliffs' evolution at both sites. Cliff melt rates varied substantially over the melt season and displayed similar patterns for all cliffs, with an overall trend of increase, peaking and then decline, on which a smaller-order variability was superimposed, controlled by snow and liquid precipitation. Cliff melt variability was driven by the combination of short- and longwave radiation and turbulent fluxes which contributed considerably during the monsoon on Langtang, when incoming shortwave was reduced (Buri et al., 2016a). Differences in air temperature at the two sites led to a general negative net longwave radiative flux on Langtang and positive on 24K. This demonstrates the need to account for the whole energy balance to estimate cliff melt.
The ice cliffs of the two study sites were generally north-facing and received little direct illumination during the study period. As a result, the aspect controls on ice cliff evolution described in previous studies (Sakai et al., 1998; Buri and Pellicciotti, 2018) were not evident when analysing the ice cliff patterns (Fig. S3), and contrary to previous observations and model tests, no evidence of melt gradient was visible at the cliff surface (Figs. S4, S5, S7, S9; Buri et al., 2016a; Watson et al., 2017b).
At both sites, the measured melt was more spatially variable than predicted by the model (Figs. S4, S5, S7, S9), which used a constant albedo and therefore was not able to account for the influence of debris on the cliff energy balance (Table 3). Two effects were visible:
Melt reduction from patchy debris. The 40 %–80 % lower measured melt values evident at the foot of Langtang cliffs 2 and 3 (Figs. 10, 12, S5d–f, S7a–c) were likely caused by the active reburial of these sections of the cliffs during shorter time intervals than the 2–3 week period over which melt was integrated. This influence of debris was also visible on the 24K cliff, where the two transects which had the higher proportion of “dirty” ice and where it was most difficult to outline the ice cliff relative to the patchy debris, experienced reduced melt. At this location, the debris on the ice cliff was thick enough to reduce melt (Figs. 14–15, S9). This melt reduction effect generally accounted for 1–3 cm d−1 relative to the locations on the cliffs that remained debris-free.
Melt enhancement from thin dust layers. The 10 %–60 % higher melt values on the upper and shallower cliff slopes that had recently become free of debris of Langtang cliffs 2–3 (Figs. S5d–f, S7a–f) were likely caused by lower albedo values due to a higher concentration of dust particles at the surface (Fyffe et al., 2020). Similarly, transect 3 of the 24K cliff was affected by small debris clasts and thin debris (Fig. 14), but these did not reduce melt and more likely led to higher melt rates due to lower albedo values.
This effect of thin debris dust on albedo was particularly visible on 24K, where cliff brightness, which we considered a proxy for albedo, followed an inverse pattern to that of cliff melt, and was therefore likely responsible for some of the observed differences between the measured and modelled melt. Indeed, a sensitivity test conducted for transect 3 on 24K showed that a 0.1 change in cliff albedo led to a 5 %–10 % change in melt (Fig. S11). Lower albedo values from this surface dust, unaccounted for in the model, could therefore partly explain measured melt rates 20 %–40 % higher than predicted by the model at the start of the study period and at peak melt on 24K. Interestingly, for the 24K cliff, changes to cliff brightness seemed to be controlled by liquid precipitation, which promoted the “washing” of the small debris clasts that accumulated at the surface of the cliffs, thereby removing the thin surface dust layer and increasing the albedo (Fig. 14, Fyffe et al., 2020). This effect was not visible on the darker, steeper and drier cliffs of Langtang, but for glaciers like 24K, it could lead to a decrease in cliff melt with the increase in occurrence of wet precipitation events at high elevation (Jouberton et al., 2022).
On the contrary, snow events at both sites in the pre- and post-monsoon periods likely reduced melt at the cliff surface. Indeed, while the snow on the debris surface usually melted away within hours after the snowfall, these north-facing steep ice slopes had the tendency to retain the snow much longer (Fig. 8f), and up to a full day on Langtang, thereby increasing the cliff albedo and interrupting ice melt until all the snow had melted. Such effects were also not represented in the model.
5.2 Controls on ice cliff area variability
One of the main results of this work was that debris local dynamics are a key influence on cliffs evolution. Debris accumulating at the surface of the cliffs influenced melt, reducing it when enough patches of debris clasts had accumulated at the surface but also darkening the cliff, therefore reducing its albedo. Debris also had an influence on cliff area and slope (Table 3, Fig. 16). Debris is constantly moving on the debris-covered surface, and this motion is enhanced by not only slope, liquid precipitation and moisture content but also debris evacuation at the base of a slope (Nicholson et al., 2018; Moore, 2018; Fyffe et al., 2020; Westoby et al., 2020). Additional debris redistribution during the wet monsoon season has even been hypothesised to increase the cliff relative area at the glacier scale (Steiner et al., 2019). While our dataset did not encompass enough cliffs to test this hypothesis, we observed considerable debris motion and areal changes at all the studied cliffs (Figs. 11b, 13b, Table 3). The planimetric area of the 24K cliff and Langtang cliff 1 did not change by more than 20 % during the study period despite evidence of cliff lateral expansion and reburial, but Langtang cliffs 2 and 3 experienced dramatic expansion and reburial, leading to doubling in size of cliff 2 within the course of a month and a reduction to its initial size 1 month later (Fig. 11b, Table 3). Langtang cliff 3 also underwent a 100 % areal increase in 2 months (Fig. 13b). These changes demonstrate the strong temporal variability of ice cliffs at the sub-seasonal scale, which underlines the interannual dynamics of ice cliff population at the glacier scale (Steiner et al., 2019; Kneib et al., 2021). Ultimately, not accounting for these geometry changes results in 5 % to 80 % discrepancies in terms of total and area-weighted cliff melt (Tables S4, S5), which has important consequences for the estimation of cliff contribution at the glacier scale, if the case that the overall cliff area would consistently increase or decrease.
Debris evacuation at the base of the slope was the main controlling factor of all the cliff area change events. For Langtang cliffs 2 and 3, the presence of a pond and its undercutting of the cliff base, led to the instability of shallow debris-covered slopes in the vicinity of the cliff, which sustained debris evacuation from the lower portion of the cliff. On the contrary, when the pond drained at the base of cliff 2, and thermo-erosional melt and instability of the cliff base ceased, this led to rapid reburial of the lower portion of the cliff. The same events were visible at cliff 1, where a cavity at the cliff base led to debris evacuation, while its absence prevented any lateral cliff expansion. For the 24K cliff, partial cliff reburial was triggered by the disconnection of the supraglacial stream from the base of the cliff, which effectively ”switched off” this sediment evacuation pathway. For the remainder of the cliff, a connection between the cliff and the stream served to maintain and sometimes steepen the slope. Undercuts at the base of ice cliffs are indeed common even without the presence of a pond (Miles et al., 2016; Röhl, 2006; Kraaijenbrink et al., 2016; Watson et al., 2017b), and streams and crevassing have been shown to promote ice cliff development by serving as mechanism for the removal of debris at their base (Mölg et al., 2020; Westoby et al., 2020; Mishra et al., 2021).
5.3 Avenues for future research
Despite the small number of cliffs covered, their similarity in aspect and the relatively short duration of the observations (one melt season), this study has highlighted the variability in ice cliff characteristics and behaviours. It has also confirmed the robustness of the Buri et al. (2016a) ice cliff energy balance model to derive cliff melt estimates for a given slope and aspect over a period of 2–3 weeks. The model, which was mostly developed and evaluated using data obtained from the Langtang catchment (Steiner et al., 2015; Buri et al., 2016a), performed well when applied to 24K, a glacier located in a very different climatic setting (Fugger et al., 2022). We could also show that using a fully static version of the model generally resulted in better melt estimates than when deriving these from pre- and post-monsoon flow-corrected Pléiades or UAV DEMs (Tables S4, S5). This confirmed the suitability of the model to explore the melt contribution of ice cliffs at the large scale. However, beyond a period of 1 month, the variability in cliff area may lead to considerable changes in cliff extents, aspect and slope and thus a need to better account for these aspects of cliff evolution in the model, even in a simplistic way (Table S5, Buri et al., 2016b, 2021). With the growing availability of high-quality multi-temporal observations of debris-covered glacier surfaces (Westoby et al., 2020; Sato et al., 2021), including from time-lapse photogrammetry, future model developments in this direction should attempt to reconcile mechanisms of cliff backwasting that are driven primarily by the cliff energy balance with debris redistribution processes and the influence of supraglacial hydrology. Models of debris redistribution exist and have been applied to understand the evolution of debris thickness patterns on debris-covered glaciers (Moore, 2021, 2018; Nicholson et al., 2018; Westoby et al., 2020). Their integration into sub-debris and ice cliff melt models, along with the representation of the influence of streams and ponds, would represent a key improvement in the numerical representation of the long-term patterns of debris-covered glacier surface evolution and melt (Bartlett et al., 2020; Ferguson and Vieli, 2021). This shows the need for the continued collection of high-spatio-temporal-resolution data of ice cliff complexes (including south-facing cliffs) and their surroundings (varying debris thicknesses). Furthermore, the cliff energy balance model would also benefit from better constraints of the characteristics and temporal variability of key parameters such as debris and ice cliff emissivity and albedo (Fig. S11), as well as a more robust interpolation of wind from the AWS to the cliff surface (Bonekamp et al., 2020). Indeed, a major uncertainty of the cliff energy balance model outlined in previous studies comes from the turbulent fluxes (Steiner et al., 2015) which are notoriously difficult to constrain on debris-covered glaciers (Miles et al., 2017a; Steiner et al., 2018). A step forward in the representation of cliff albedo variability could also be to extract it from the brightness observations of the time-lapse images (Corripio, 2004) and the precipitation patterns, although the difficulty here will be the transferability of such a relationship from glacier to glacier.
This study considerably improved our understanding of ice cliff evolution by using terrestrial time-lapse photogrammetry to quantify the weekly evolution of four ice cliffs on two climatically contrasting Himalayan debris-covered glaciers. Notably, the time-lapse camera DEMs enabled a precise quantification of the cliff melt by accounting for sub-seasonal cliff geometry changes, which are ignored when extracting melt from pre- and post-monsoon or annual DEMs. Prior to our work, cliffs had been observed only at the beginning and end of the melt season (because of logistical and field challenges), but never during this period, when most of the ablation occurs.
We found that the sub-seasonal variability in cliff melt was high and was driven mainly by shortwave radiation, while air temperature was the determining factor for the sign of the net longwave contribution. Overall, the modelled melt agreed with the observations. On the other hand, the interaction of the cliffs with surrounding debris-cover was found to be particularly crucial and increased the spatial variability of the cliff melt by causing very strong changes in the cliff geometry. At the cliff surface, it had two main effects:
The presence of small clasts or thin layers of dust reduced the cliff albedo (resulting in increased melt). Liquid precipitation events were effective at washing this thin debris-cover from the cliff surface and increasing its albedo, whilst snow events had a similar effect.
The presence of slightly thicker, often patchy debris at the cliff surface and the active reburial of parts of the cliffs reduced melt via the debris insulating effect.
Ultimately, our results confirmed that the connectivity between ice cliffs and supraglacial hydrology (streams, ponds) exerts an important control on rates and patterns of cliff expansion and reburial and that the relevant processes and feedbacks need to be accounted for in contemporary ice cliff energy balance models to better constrain cliff melt and the long-term surface evolution of debris-covered glaciers.
The Python scripts to automate the processing of the time-lapse images to DEMs and the R scripts to calculate melt are available on Zenodo (https://doi.org/10.5281/zenodo.7044364, Kneib et al., 2022) and GitHub (https://github.com/MarinKneib/TimeLapse_photogrammetry, last access: 9 November 2022).
The supplement related to this article is available online at: https://doi.org/10.5194/tc-16-4701-2022-supplement.
MK, ESM and FP designed the study. MK and ESM designed the time-lapse setup. MK, ESM, SF and MM conducted the fieldwork on Langtang, and MK, ESM, SF, TES, ZC, MT, MJW and WY on 24K. PB provided the cliff energy balance model and helped in applying it. ESM provided the codes to flow-correct the different DEMs and helped in applying them. MK completed all the analysis and composed the manuscript. FP supervised the study. All authors aided in the reviewing and editing of the manuscript.
The contact author has declared that none of the authors has any competing interests.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
The Langtang Pléiades images were acquired by CNES's ISIS programme facilitating science access to imagery. We would like to thank Simone Jola, Stefan Boss and Marco Collet at the Swiss federal research institutes SLF and WSL for their help with the assembling and the testing of the time-lapse camera setups. Thanks go to Hamish Pritchard for sharing with us the Langtang ice thickness data and to the Agisoft team for their support. The weatherproof box and intervalometer were purchased from Bixion, whose team provided very helpful advice for the installation and wiring of the time-lapse cameras. Last but not least, the fieldwork was supported and organised by the Himalayan Research Expedition (HRE) team in Nepal, and Tibetan helpers Labadunzhu and Wangqingduojia in Tibet, who made the instrument installation and data collection possible.
This research has been supported by the H2020 programme of the European Research Council (RAVEN (grant no. 772751)) and the Royal Geographical Society (grant no. NA170325).
This paper was edited by Kang Yang and reviewed by Duncan J. Quincey and one anonymous referee.
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