Mapping Glacier Forelands Based on UAV BVLOS Operation in Antarctica

: The aim of this article is to show geomorphological mapping of remote Antarctic locations using images taken by a fixed ‐ wing unmanned aerial vehicle (UAV) during the Beyond Visual Line of Sight (BVLOS) operations. We mapped landform assemblages developed in forelands of Ecology Glacier (EGF), Sphinx Glacier (SGF) and Baranowski Glacier (BGF) in Antarctic Specially Protected Area No. 128 (ASPA 128) on King George Island (South Shetland Islands) and inferred about glacial dynamics. The orthophoto and digital elevation model allowed for geomorphological mapping of glacial forelands, including i) glacial depositional landforms, ii) fluvial and fluvioglacial landforms, iii) littoral and lacustrine landforms, iv) bodies of water, and v) other. The largest area is occupied by ground moraine and glacial lagoons on EGF and BGF. The most profound features of EGF are the large latero ‐ frontal moraine ridges from Little Ice Age and the first half of the 20th century. Large areas of ground moraine, frequently fluted and marked with large recessional moraine ridges, dominate on SGF. A significant percentage of bedrock outcrops and end moraine complexes characterize BGF. The landform assemblages are typical for discontinuous fast ice flow of tidewater glaciers over a deformable bed. It is inferred that ice flow velocity decreased as a result of recession from the sea coast, resulting in a significant decrease in the length of ice cliffs and decrease in calving rate. Image acquisition during the fixed ‐ wing UAV BVLOS operation proved to be a very robust technique in harsh polar conditions of King George Island.


Significance and Aim of the Study
Retreat of the Antarctic Peninsula ice sheet, observed since the mid-20th century, is attributed to atmospheric warming of approximately 2-3°C [1,2]. In recent decades, hundreds of glaciers draining the Antarctic Peninsula, and adjacent islands have undergone general retreat, having direct and immediate effects on progressive development of their foreland environments [2,3]. Marginal zones of Antarctic glaciers are considered an important indicator of global climate change [4] due to the extremely high rates of recent environmental changes and the sensitivity of polar terrestrial ecosystems [5]. A relevant example of trends in terrestrial ice cap fluctuations is observed on King George Island (KGI), located 120 km from the northern tip of the western coast of the Antarctic Peninsula in the South Shetland Islands (Figure 1).
Only about 10% of KGI's surface (138 km 2 ) is ice-free, and the ice cover consists of three main ice domes and seventy glacier drainage basins [6]. The highest elevation reaches slightly more than 700 m a.s.l. at a dominating central dome. The glaciers flow radially out of the domes and terminate at the sea coast or slightly inland. As reported by Simões et al. [6], retreat of the glacier fronts between 1956 and 1995 caused a reduction of 7% (89 km 2 ) of the total ice-covered area. A more recent study of Rückamp et al. [7] shows that between 2000 and 2008 the loss of glacierized surface amounted to about 20 km 2 (about 1.6% of the island area). The area of glaciers flowing east from Warszawa Icefield (southern ice dome of KGI) to Admiralty Bay, the main inlet from the SE, shrank by 31.3% in years 1979−2018 [8].
Changes in the glacial system affect the nearby land ecosystems in many ways. Recently deglaciated landscapes undergo rapid geomorphic as well as biologic changes [5,9,10]. High sediment loads originating from paraglacial erosion of recently exposed landforms are quickly delivered to the coastal zone [9,[11][12][13].
Antarctic Specially Protected Area No. 128 (ASPA 128), located on the west coast of Admiralty Bay in the vicinity of the Henryk Arctowski Polish Antarctic Station (Arctowski), hosted extensive geomorphological research in years 1990-1992 during the Polish expeditions to KGI [14−16]. Since that time, the glaciers underwent significant recession [8]. In recent years, due to developments in remote sensing, mainly unmanned aerial vehicle (UAV) technology and terrestrial laser scanning, several geomorphological studies were performed in this area. They focused on periglacial landforms on Demay Point peninsula [17], glacial dynamics and foreland development of Ecology Glacier [18] and Baranowski Glacier [13], and volcanic landforms on Penguin Island [19]. Recession of all of the glaciers in the area since 1979 was well documented by Pudełko et al. [8], but an overall geomorphological study of contemporary glacial forelands in ASPA 128 has been lacking. The aim of this study is to fill this gap by determining the area and spatial distribution of glacial landforms sensu lato developed on main glacial forelands in the area, namely Ecology Glacier foreland (EGF), Sphinx Glacier foreland (SGF) and Baranowski Glacier foreland (BGF) (Figure 2). We used aerial photographic images taken by a fixed-wing unmanned aerial vehicle (UAV) during the Beyond Visual Line of Sight (BVLOS) flights, followed by Geographic Information System data processing to detect and quantify the landform assemblages.
The BVLOS fixed-wing UAV operations allow us to cover a significantly larger surface and gather high-resolution images (with a higher resolution for KGI area than available with commercial satellite images) in one flight in comparison with the Visual Line of Sight operations that usually utilise rotary-wing UAVs. In remote, difficult-to-access polar locations, BVLOS UAV operations allow for multifaceted environmental analyses far away from a polar station, saving time and logistic efforts [19,20]. Recent developments in polar UAV operations, including Antarctic missions, are described in Zmarz et al. [19] and Bhardwaj et al. [21].

Characteristics of the Study Area
The study area was located in ASPA 128, western coast of Admiralty Bay, King George Island, South Shetland Islands, West Antarctica (Figures 1,2). It is a big lowland ice-free area (about 16.8 km 2 ), covered by diverse tundra communities [22], constituting a favorable place for huge breeding colonies of marine birds and pinnipeds [23]. Bedrock is generally composed of basaltic and andesitic lavas, interstratified sediments of Eocene-Oligocene age and some Pleistocene plugs and dikes [24]. Northern latero-frontal moraines of Ecology Glacier ( Figure 2) are deposited against basalts and andesites alternating with breccias and tuffs (Arctowski Cove Fm.). Between Ecology Glacier and Sphinx Glacier the bedrock is composed of tholeiitic and subordinately andesitic lavas with pyroclastic intercalations (Llano Point Fm.). Southern latero-frontal moraines of Baranowski Glacier are deposited against porphyritic lavas, tuff-breccias, siliceous pisolites, conglomerates and lapilli tuffs (Demay Point Fm.) [24]. Bedrock is overlain predominantly by glacial ice and sediments deposited by the glaciers and meltwaters, weathering and slope sediments and marine sediments, which compose raised terraces, a contemporary beach and a storm ridge [15,25].
The climate of the study area is polar maritime [26] with some participation of continental air from the south [27] resulting in highly dynamic weather conditions. The mean annual air temperature (MAAT) calculated for joined periods 1977−1999, 2006−2007 and 2012 is −1.5°C [28]. An increase in MAAT by 1.2°C occurred for the period of 1948-2011 on KGI [29], which resulted in retreat of local glaciers [16,30,31]. However, a set of end moraines developed at the contemporary margin of Baranowski Glacier and recent deceleration of glacial surface lowering [18] can be attributed to a slightly negative temperature trend observed since the beginning of the twenty-first century [32]. Thermal conditions result in the permafrost table depressing well below 1.0 m or even absent at altitudes close to sea level and glacier forelands [33,34]. This allows for free circulation of glacial melt water. Glacial lagoons receive water from glaciers, tides and relatively abundant precipitation. Tide amplitude is usually about 1.5 m [35], which results in a well-developed beach and a storm ridge.
According to Marsz and Styszyńska [27], the mean annual precipitation for the period 1978-1996 was 505.7 mm and mean annual number of rainy days was 205. The snow cover is highly variable, and sometimes snow cover can melt almost completely, even in winter [36], but may also appear after summer snow storms. Average annual wind speed equals 6.6 ms −1 [32] with frequent wind gusts sometimes exceeding 65.0 ms −1 [11,37]. Storms are typical climate elements in the region, which makes the use of UAV difficult and risky.
Ecology Glacier, Sphinx Glacier and Baranowski Glacier flow east from Warszawa Icefield, the plateau of which lies between 400 and 460 m a.s.l. Their equilibrium line altitude in the 21st century varied between 156 m a.s.l. in 2012/2013 [38] and 290 m a.s.l. in 2006/2007 [8]. Since the first availability of aerial images, taken in 1978/1979 [39−41], the glaciers snouts retreated by a distance from 260 m (Baranowski Glacier) to 740 m (Ecology Glacier). Glacier forelands in places inundated by lagoons constitute a significant part of ASPA 128. Retreat rates of the glaciers slowed down, following recent climatic cooling [18,32].

Data Acquisition
The Beyond Visual Line of Sight (BVLOS) flights were performed using the PW-ZOOM fixedwing UAV [19,42] designed, manufactured and tested at the Warsaw University of Technology in Poland. The airplane was equipped with an automatic control system (autopilot) linked with a telemetry module. A similar module was used in the Ground Control Station, which was connected to a computer running special software HORIZONmp (MicroPilot, Stony Mountain, Canada) for planning the flight path and managing the UAV flight. The flight was therefore autonomous, although at any time it could be interrupted by sending the order to return to the base.The operation was performed on 15˗17 November 2016 by a three-person team: the remote control pilot, the ground control station operator and the technical operator (all had BVLOS licenses issued by national authorities).
The photogrammetry grid was designed over the west coast of Admiralty Bay and the forelands of retreating glaciers (Figures 2,3) with starting and landing points near Arctowski. The distance between the grid lines was ~ 73 m, which provided 70% forward and side overlap, the length of the lines was 7500 -10000 m and flight altitude was 500 m a.s.l. The images were gathered in three flights 7h in total, covering a distance of 720 km (Table 1).  Using UAVs to collect environmental data is a quite new phenomenon in Antarctica; therefore, guidelines for safe UAV use are currently being developed (e.g., COMNAP RPAS Handbook of the Council of Managers of National Antarctic Programs; COMNAP). The authors of this paper had to meet certain obligations, such as preparing an Environmental Impact Assessment, obtaining permits for taking or harmful interference of Antarctic fauna and flora and providing information needed for information exchange between parties to the Antarctic Treaty. All parties conducting operations on KGI, as well as the International Association of Antarctica Tour Operators (IAATOs), were informed about our UAV operation. A chain of communication was pre-agreed with Base Frei (Chile), which controls flight operations on KGI.

Data Processing
The images were obtained in RAW format during the flight and converted to JPEG format in Digital Photo Professional version 3.13.0.1 (Canon INC) software. All images had georeferences (X, Y, Z) registered by the autopilot logger mounted on the UAV. For geolocation of images, the GPS Receiver GP-E2 with 1575.42 MHz frequency was used, which allowed for horizontal accuracy < 5m. To estimate vertical accuracy, a reference measurement taken near the Arctowski station was used (a concrete pillar named Jasnorzewski Point). The data were obtained by continuous GPS measurements and other two ground control points (GCPs), marked in Based on the orthophoto and DEM, the landforms were manually determined by vectorization in ESRI ArcGIS 10.3 software at varying scales. Patches of relatively uniform landforms or bodies of water (e.g., outwash, ground moraine, glacial lagoon, and patches of repetitive landforms, e.g., recessional end moraine ridge complex) were vectorized in a relatively small scale (1: 1000) but, in places, individual objects such as a snow patch, an esker or a drumlin required more detailed mapping at a scale of 1: 500. During our UAV missions the snow patches were relatively abundant, which inhibited geomorphological interpretation of UAV images. Due to this we did not map the southernmost foreland of Tower Glacier and Windy Glacier ( Figure 2).
Our geomorphological mapping was not based on DEM segmentation, but solely on image classification based on our geomorphological experience acquired in different glacial forelands and studies of relevant literature (see Discussion). Main characteristics of landforms (area, shape, association with other landforms) and justification of their determination are presented in Results.

General Characteristics and Quantification of Landforms
The general geomorphological mapping included the following units: glacial depositional landforms, fluvial and fluvioglacial landforms, littoral and lacustrine landforms, bodies of water (lakes, lagoons and rivers), glacier ice (marginal parts of glacier) and snow patches, bedrock and other surfaces not recognized or not associated with glaciers ( Figure 4). Bedrock includes both glacially eroded landforms and coastal rocky outcrops because we were unable to distinguish between surfaces of glacial abrasion, quarrying or coastal abrasion. Rock surfaces of residual hills and taluses, and not recognized landforms outside of glacial forelands, were named "bedrock" or "other", respectively. It is frequently difficult to determine the lateral boundary of glacier forelands, especially in case of adjacent glacier tongues or lobes (e.g., the southern limit of EGF). Therefore, we decided to limit our analysis to rectangular frames ( Figure 4). The frames for SGF and BGF are slightly overlapping in order to show immediate surroundings of both forelands, but we calculated the statistics provided below ( Figure 5) taking into account the crest of a medial moraine ridge. Glacial depositional landforms cover most of the forelands' area: 472,867 m 2 on EGF where they constitute 45.3% of mapped landforms (excluding snow patches and "other surfaces"), 524,459 m 2 (73.2%) on SGF and 508,749 m 2 (53.9%) on BGF ( Figure 5).

Landform Characteristics
Below we present characteristic features of landforms mapped in detail on forelands of Ecology Glacier, Sphinx Glacier and Baranowski Glacier ( Figure 6) with a short interpretation. This group includes old and young latero-frontal moraine complexes, lateral and medial moraine ridges, recessional end moraine ridge complex, large recessional moraine ridges, ground moraine with annual push/stagnation moraines, fluted end moraine complex and bulldozed end moraine complex.
The old latero-frontal moraine complex marks the outer margin of glacier forelands, possesses a curved shape and is best developed in EGF, where it creates a continuous belt over a distance of about 1000 m (Figure 7). The moraines are up to 12 m high with depressions overgrown by shallow tundra (Figures 7A,8A) and host small lakes. The young latero-frontal moraines are much higher (up to 40-50 m) and are ice-cored according to Rachlewicz [16] and Kostrzewski et al. [14,15]. On aerial images they can be easily distinguished from the older moraine complex by much sparser vegetation ( Figures  7,8A).
Lateral moraines are relatively short and straight running ridges, disconnected from the laterofrontal moraine complex. We mapped them only in the northern part of SGF and the southern part of BGF (Figures 9,10).
A medial moraine ridge developed between Sphinx Glacier and Baranowski Glacier has been named Błaszyk Moraine [40,44]. It is very long (1150 m), wide (up to 250 m) and over 100 m high at its western part, towards its origin at Zamek hill (Figures 2,8B,9,10). It has been already well visible in aerial images from 1978/1979 [40], which testifies to its relatively old age.
Recessional end moraine ridge complexes are arch-shaped patches of moraine ridges parallel to the glacial front, relatively long and frequently spaced. They are developed in the northern part of EGF, between 250 and 580 m away from the contemporary glacial front (Figure 7).
Large recessional moraine ridges are individual landforms, between 15 and 65 m long and 3 to 8 m wide, best developed in the distal part of SGF (Figures 9,9A). Sometimes a distinctive pattern of clear-cut small ridges running parallel to the glacier margin is seen on the ground moraine and interpreted as annual push/stagnation moraines. The small ridges are best developed immediately south of the glacial lagoon on EGF (Figures 7,7D), close to the Sphinx Glacier front ( Figure 9) and north of the lagoon on BGF (Figure 10). The ridges are usually between 10-30 m long, 1.0-2.5 m wide and spaced 5 to 10 m from each other.
The fluted end moraine complex is developed only in the central and southern parts of the BGF within the first 100 m distance for the contemporary glacial front, but separated from the glacier by a narrow 20 to 40 m wide belt of the bulldozed end moraine complex ( Figure 10). The fluted end moraines are spaced between 5 to 15 m and are about 5m wide ( Figure 10D). The flutings allow to infer that the moraine complex was deposited due to submarginal freeze-on and emplacement of fluted sediment slabs [45].
The bulldozed end moraine complex consists of narrow parallel ridges adjacent to the glacier margin with no flutings ( Figure 10A). Lack of fluting allows to infer that the dominant process of deposition was bulldozing of proglacial sediments. Both complexes of end moraines (fluted and bulldozed) do not exhibit sawtooth planform geometries, which are typical for tensile-fractured glacial snouts [45−47].

Ground Moraine Complex
This group of landforms includes ground moraine, fluted moraine, fluted moraine with crevasse-fill ridges and drumlins.
The ground moraine was mapped in places of relatively smooth surface ( Figure 10B). In places (e.g., eastern part of SGF) one can notice small-scale ridges, which can be interpreted as remnants of annual push/stagnation moraines or crevasse-fill landforms. However, they are not clearly seen on orthophoto and DEM; therefore, we applied the general term of ground moraine in such cases.
The fluted moraine possesses a characteristic pattern of streamlined ridges (flutes) and grooves and occurs commonly in interior parts of glacial forelands, which is a common situation in other glacial land systems [48−50]. Some flutings are developed on a lee side of an anchored boulder, and some are segmented. In the southern parts of EGF and SGF the flutings are sometimes overlain with diagonal (ice-flow oblique) pattern of small ridges, 5 to 50 m long and 1.2 to 5 m wide ( Figure 7C), which are interpreted as crevasse-fill ridges.
Based on analyses of length, width and elongation ratios of 165 vectorized, streamlined, longitudinal landforms developed in studied forelands, we distinguished two drumlins on EGF (E1 and E2) and three on SGF (S1 -S3) (Figures 7,9). For further information about morphometric characteristics of flutes and drumlins see Discussion (Section 4.3, Figure 11, Table 2).
In some places, especially in the northern part of EGF (Figure 7), a dense network of erosional gullies developed on morainic slopes and were mapped as areas of paraglacial erosion. The gullies are up to 100 m long, and the largest vectorized polygon (on EGF) occupies 19,147 m 2 . They constitute an important source for outwash material and testify to significant paraglacial reworking of glacial sediments [9]. Surface wash valleys are shallow bowl-shaped valleys developed between glacial forelands (Figures 4,7,9) and mapped by us in order to allow for better spatial orientation. They originate from fluvial erosion of snow melt and rain waters.
The largest fluvioglacial landforms are outwashes, which cover a similar area in each of the forelands: 89,739 m 2 on EGF, 101,541 m 2 on SGF and 95,768 m 2 on BGF. Stripes of outwash can usually be found in depressions within ground moraine, parallel to the glacier margins (Figures 7,9,10). Eskers are poorly developed and create simple sinusoidal ridges, up to 65 m long and 5 m wide ( Figure 9C). There are only two very small patches interpreted after Sziło and Bialik [13] as kames on BGF, between storm ridge and outwash ( Figure 10).

Littoral and Lacustrine Landforms
Sea beach constitutes an almost continuous strip of land (Figure 4), between 10 and 60 m wide, adjacent to the sea, interrupted in places by rocky outcrops (e.g., on BGF; Figure 10). Sand bars developed on EGF and BGF, protecting sea water from easy access to glacial lagoons in a dynamic coastal environment (Figures 7,10) [35]. Directly behind the beach there is a clearly visible strip of land that we interpret to be a storm ridge due to its dryer surface in comparison with the beach (Figures 7,9,10). On EGF and BGF, coastal landforms smoothly evolve into lacustrine strandflats developed around shorelines of glacial lagoons (Figures 7,10).

Bodies of Water
The largest body of water is by far the glacial lagoon on EGF (251,257 m 2 ), which demarcates a 621 m long tidewater ice cliff of Ecology Glacier (Figure 7). There is also a smaller lagoon (62,736 m 2 ) at Baranowski Glacier (Figure 10), resulting in a much smaller (46 m long) direct contact between water and the glacial front.
Lakes occupy comparable areas in the studied forelands, between 10,517 m 2 (SGF) and 16,159 m 2 (BGF) (Figures 7,9,10). Most of the lakes are bodies of relatively stagnant water, except for one transfluent lake in BGF located at the confluence of two glacial rivers (Figures 8C,10).
We mapped active river channels only where river water could be seen. The width of the marked channel depicts the river bed (contemporary filled with water) together with adjacent bars, which were dark on the images due to high water content (Figures 7,9,10). In the southern part of SGF the active river channel disappears downstream, which allows us to infer that river water percolates down into alluvial sediments marked as outwash (Figure 9).

Snow Patches, Bedrock and other Surfaces
There were numerous snow patches varying greatly in size during austral summer of 2016 when the UAV images were obtained. Snow caused major problems in mapping of SGF because the glacier area did not differ from proglacial snow patches in terms of color and texture (Figure 9). Bedrock is far more present on BGF due to the outcrops at the former nunatak Siodło, two peninsulas (Agat Point and Block Point) as well as the northern escarpment of Demay Point along the southern margin of BGF (Figures 8C,10).

BVLOS Data Acquisition and Interpretation
Studies in the Antarctic environment are frequently performed in remote ice-free areas (oases) or islands, which are not easily accessible [51]; therefore, systematic terrestrial surveys are usually limited to small areas located in the vicinity of research stations [52,53]. This can be overcome by the use of the BVLOS fixed-wing UAV flights [17,19].
However, BVLOS flights are still seldom used in geomorphological studies, despite the development of autonomous controllable micro-airplanes technology and platforms designed to work effectively in harsh Antarctic environments [54,55]. For example, our PW-ZOOM plane tolerates strong, unpredictable Antarctic winds up to 23 ms -1 [42] and still performs high-quality photogrammetric flights [17,19,43]. The BVOLS fixed-wing UAV operations allow to cover a significantly larger surface in comparison with rotary-wing UAVs, which are frequently used in a variety of geomorphological studies [45,49,56−63].
In remote areas of the Antarctic environment, where the placement of the ground control points (GCPs) is impossible or requires a lot of time and logistics, the BLVOS operations offer a good solution (in our case, we used GCP, which was located near the Arctowski station, Jasnorzewski Point). The horizontal accuracy of the objects seen on images obtained in our study is limited by the accuracy of the GPS receiver mounted on the UAV (< 5m). This can be a problem in repetitive highprecision mapping (e.g., in monitoring erosion [57,58]), but it is sufficient in determining landform assemblages and calculating their area, aspect or other parameters [17,19].

Glacial Dynamics
The studied glacier forelands differ between themselves most importantly in the length of ice cliffs and the size of glacial lagoons, which significantly influences calving rate and frontal recession. Ice thickness of the frontal parts of Ecology Glacier, Sphinx Glacier and Baranowski Glacier does not exceed 100 m, and ice flow velocities are below 100 m yr -1 [64], which leads to their classification as normal glaciers (not fast glaciers) [12,65,66]. However, the landform assemblages observed could be inherited from discontinuous fast ice flow of tidewater glaciers [67], which probably occurred when ice was thicker, had more direct contact with seawater and calving rate was higher. Such glaciers developed bed-flow type landform assemblages with push moraines in land-based parts (N segment of EGF), flutes and drumlins on the ground moraine behind glaciers margins, which either developed terrestrially (EGF) or in the sea (SGF, BGF). A deformable bed is present on the west coast of Admiralty Bay, constituted by soft sediments [16,68] and probably high pore water pressure due to low elevation above sea level and shallow bedrock inhibiting downward percolation of meltwaters. This would decrease the shear strength of subglacial sediments and facilitate fast ice flow and deformation of subglacial sediments [12,69−71].
The thermal structure of the studied glaciers is yet unknown, and most probably underwent change since the onset of climate warming in the 20th century. Polythermal and temperate glaciers are present on KGI [72,73], although no indirect evidence of temperate (or polythermal) state of ice was observed, such as winter sub-or englacial water discharge or icings [11,27]. Poor development of eskers (short curved ridges, not segmented) allows only limited interpretation of the routing of glacial melt water within the glaciers, probably in subglacial tunnels [12]. The thermal structure (probably polythermal) and significant amount of coarse-grained sediments, like marine gravel found in glacial sediments of EGF, SGF and BGF [16], did not inhibit fast ice flow and formation of flutings and drumlins [48], especially when the glaciers extended to the coastline where calving facilitated fast flow of glacial ice. Changes in ice flow velocity most probably resulted from calving events, which temporarily distorted the pressure equilibrium between an ice-cliff and seawater, and triggered faster ice flow [74]. Following ice mass loss, glaciers thinned and largely retreated on land. The flutes testify for unsteady basal slip velocity and basal water pressure [50].
There are no well-documented events of glacial surges of the studied glaciers. However, according to Birkenmajer [24] between 1950 and 1977 Ecology Glacier and Baranowski Glacier probably surged over coastal storm ridges and beaches forming push moraines, which we named young latero-frontal moraine complexes. Extensive flutings and crevasse-fill ridges could be inherited form surge events [75,76].
Significant retreat of the glaciers since 1979 created landform assemblages, which testify for frontal recession with glaciers maintaining their integrity and not turning into blocks of dead ice. Ground moraine complex is not covered by landforms associated with aerial disintegration of glacier such as kames, kame terraces and kettle-holes [12].

Flutings or Drumlins?
The shape and origin of subglacial streamlined ridges (flutes and drumlins) has received considerable attention in geomorphological research conducted almost exclusively in the northern hemisphere [12,49,[77][78][79][80][81][82]. Landforms, determined by us as drumlins, create distinctive two groups separated from flutings on the length-to-width diagram ( Figure 11A). Either their width is significantly greater (E1, E2 and S1-S2) or length (S1-S3). On the length-to-elongation ratio diagram ( Figure 11B) the boundary between the flutings and the drumlins is shown by the dashed line, which cuts-off the landforms of lowest elongation ratio, except for landform S3. Figure 11. Length-to-width (A) and length-to-elongation ratio (B) diagrams for 165 analyzed flutings and drumlins (note that the axis scales of the diagram B are logarithmic); drumlins are marked E1 and E2 (Ecology Glacier foreland) and S1-S3 (Sphinx Glacier foreland).
Our designation of drumlins is in accordance with findings of Clark et al. [82] who discovered that the maximum elongation ratio of drumlins scales with their length ( Figure 11B, Table 2). However, only drumlins in EGF (E1 and E2) fit to the equation determined by Clark et al. [82]: where Emax is the maximum elongation and L is length. Very long (>100 m) longitudinal landforms on SGF (S1-S3) could be called megaflutes instead of drumlins [80]. However, we decided to name them drumlins due to their outstanding length and significant width in comparison with flutings ( Figures 11A,B) and to avoid extra entities in the already complex map legend ( Figure 6). Contrary to the most widely accepted cavity-infill model [12,77,79] in EGF, SGF and BGF, only some flutes start at the lee side of boulders, suggesting basal ice crevassing [78] or melt-out of longitudinal thickenings of basal debris-rich ice [81].

Ecology Glacier Foreland
The most profound features of EGF are the large old and young latero-frontal moraine ridges, which can be traced along the margin of the foreland, and the large glacial lagoon. The old laterofrontal moraines were deposited during the Little Ice Age (LIA) glacial maximum, which ended in this region around AD 1850 [31,83]. The young latero-frontal moraine complex has developed in the 20th century, before 1979 when the rapid deglaciation started [31]. However, in 1989 they were still very close to the glacier front, and the ice cliff was still at the open waters of Admiralty Bay [8]. The more frontal parts of both morainic complexes are of push origin, which can be inferred from their structure, beach material and whaling artefacts from the first decades of 20th century and artefacts from the 1950s embedded within glacial till [16,24].
The lagoon plays a significant role in shaping the pattern of glacial retreat. The glacial cliff retreats fastest, producing two characteristic concavities: one in the northern side, another in the southern part of the glacial cliff. According to Pętlicki et al. [18], the glacial lagoon depth in these places is 5-8 m, while in the central part of the glacial cliff where glacial retreat is slower, the depth of the lagoon is less than 2 m. It is probable that the sand bar closing the lagoon is deposited on a subaqual moraine built at the former grounding line [84].
Highly negative mass balance over 1979-2016 resulted in ice elevation change rate in the ablation area between -1.  [8,18]. The recent deceleration of retreat [18] has probably resulted in the formation of annual push/stagnation moraines in the northern part of the glacier margin ( Figure  7).

Sphinx Glacier Foreland
The surface area of Sphinx Glacier is probably smaller than on our geomorphological map (Figure 9), due to abundant snow cover present on the glacier and along its margin during data acquisition. On the orthophoto of Pudełko [40] two separate lobes (northern and southern) divided by the Czajkowski Needle nunatak are visible ( Figure 2). A later publication [8] shows satellite images taken on 13 February and 10 March 2018, in which the glacier is clearly divided into the northern and southern, more fractured lobe ( Figure 2). Our images display some dark surface between the two lobes, which we interpreted as medial moraine, bedrock outcrops or fluted moraine.
The most characteristic geomorphic features of SGF are large areas of ground moraine. Fluted moraine characterizes more proximal parts of the foreland (deposited after 2011), and numerous large recessional moraine ridges in a more distal parts (last two decades of the 20th century) together with relatively well-developed drumlins [8].
There is a characteristic pattern of outwash, which is predominantly deposited in shallow valleys within the ground moraine running perpendicular to the front of the northern lobe.
Sphinx Glacier reached open sea during the LIA maximum along its whole frontal margin, as there is no evidence it was enclosed by in land-based latero-frontal moraines. An ice-cliff must have resulted in calving, which in turn facilitated relatively vast ice flow. Between 1979 and 2016 the glacier receded by about 380 m in its southern part and only about 190 m in its northern part. This means an average recession rate between 5 and 10 m yr -1 , which is much slower than that of Ecology Glacier and can be explained by the absence of a glacial lagoon.

Baranowski Glacier Foreland
The Baranowski Glacier foreland is clearly divided into the northern and the southern lobes divided by a former nunatak called Siodło (Figure 2). The northern lobe receded between 1979 and 2016 by about 620 m, indicating a mean annual rate of recession 17 m yr -1 . The southern part of the southern lobe receded only by about 240 m (6.5 m yr -1 ). This asymmetry is caused by the influence of calving along the ice cliff of the northern lobe. Furthermore, along the margin of the southern lobe there is a very well-developed complex of contemporary end moraines, probably linked with the recent climatic cooling.
The ground moraine complex is visible in front of the two lobes and possess a typical structure with fluted moraine in the more proximal part of the foreland and ground moraine (not fluted) in the more distal part [48−50]. A belt of outwash developed in an arch pattern separates the fluted moraine from the ground moraine.
The end moraine complex probably resulted from the recent (since 1998/1999) climatic cooling [32] and slowing of glacier retreat. The change of the character of end moraines at the southern part of the glacier from fluted to bulldozed allows to infer that there was a change in a mode of deposition from subglacial freeze-on and stacking of sediment slabs to bulldozing of soft sediments [12,45,85]. However, due to the complexity of these processes, the analysis based solely on images obtained preclude further inference.

Conclusions
Image acquisition by fixed-wing UAV PW-ZOOM proved to be a robust technique in harsh polar conditions of marine Antarctica. The images obtained allowed to save time required for a popular approach of using rotary UAV platforms. We argue that photogrammetric UAV BVLOS flights provided high-quality data, much better than satellite imaging, and should be regarded as a suitable tool in gathering geomorphological data in remote polar locations. The high-resolution orthophoto with DEM allowed for detailed vectorization of landforms in glacial forelands.
As all mappings based on remote sensing, our mapping also suffers from some uncertainties. These result from snow patches and too low image resolution to distinguish certain landforms (e.g., glacially abraded rock surfaces typical of whalebacks or roche moutonnée could not be detected). The glaciers receded substantially since the last extensive geomorphological studies, exposing vast new foreland area; therefore, more in-field work would be necessary to support our photointerpretation. Geomorphological fieldwork would be necessary to verify our interpretation in certain places (e.g., crevasse-fill origin of some ridges). The issue of kames would also require verification, as we could map them only on one foreland based on a former study because no clear and determining feature was visible on our images. It would be especially interesting to check the internal structure of fluted and bulldozed end moraines developed on BGF as these landforms may testify for most contemporary glacial dynamics.
The studied glacial forelands host landform assemblages typical of discontinuous fast ice flow of tidewater glaciers over deformable beds, which results in large latero-frontal push moraine complex, flutes and drumlins. Ice flow velocity decreased as a result of recession from coastline (most rapid after 1979), resulting in significant decrease in the length of ice cliffs and glacier cover thinning. Glacial lagoons are responsible for asymmetric recession of Ecology Glacier and Baranowski Glacier fronts. Frontal recession for the last forty years revealed ground moraine complex marked with flutings, drumlins, annual push/stagnation moraines and crevasse-fill ridges. The fluted and bulldozed end moraine complexes developed near the front of the southern lobe of Baranowski Glacier are attributed to recent climatic cooling.