The glacial geomorphology of sub-Antarctic Marion Island

ABSTRACT

Since the discovery of glacial features on sub-Antarctic Marion Island, the character and extent of a historic glacial period have remained an important research focus for earth science investigations. Previous glacial reconstructions were limited to mostly pre-GPS field observations and pre-digital mapping through a Geographic Information System. With the aid of GPS field mapping, high-resolution satellite imagery and a digital surface model with a 1 × 1 m cell resolution, this paper provides a comprehensive, geo-rectified spatial geodatabase and map of Marion Island’s glacial geomorphology. The geodatabase includes an inventory of glacial erosional (e.g. striations) and depositional (e.g. moraines) features compiled from existing records as well as new features mapped from recent field observations. The final map and the geodatabase, which is downloadable as ESRI layer-package files, will aid future field investigations and modelling applications to understand Marion Island’s Quaternary landscape evolution and post-glacial ecological succession.

KEYWORDS:

• Sub-Antarctic
• Marion Island
• glacial geomorphology
• mapping
• palaeo-ice extent
• Quaternary landscape evolution

1. Introduction

For paleoclimate studies of the Southern Hemisphere, the sub-Antarctic Islands act as important sentinels of the nature and timing of Quaternary glaciations (e.g. Hodgson et al., 2014; Schaefer et al., 2015). The glacial geomorphological records preserved on these islands provide valuable insights into earth systems response to hemispheric climate change (Hodgson et al., 2014; Jomelli et al., 2018; Rainsley et al., 2019; White et al., 2018). At an island-scale, glacial reconstructions aid to further our understanding of local rates of ecological succession and landscape evolution (e.g. Hodgson et al., 2014; Jomelli et al., 2018; Rudolph et al., 2020; White et al., 2018). Such glacial chronological studies and reconstructions rely heavily on process-form interpretation(s) and spatial representation i.e. mapping of the glacial geomorphological record (e.g. Bendle et al., 2017; Chandler et al., 2018). Sub-Antarctic Marion Island (46°54’S, 37°45’E) is one of the few islands in the southern Indian Ocean sector that can facilitate our understanding of glacial oscillations in this region (Boelhouwers et al., 2008; Hodgson et al., 2014; Nel et al., 2021). As on other sub-Antarctic islands, past glaciations have had a significant influence on the evolution of Marion Island’s landscape (e.g. Hall et al., 2011; Hedding, 2008; Kent & Gribnitz, 1983; Sumner & Meiklejohn, 2004) and ecological succession (e.g. Chau et al., 2019; Mortimer et al., 2012; Scott, 1985; Scott & Hall, 1983). Although some advancement has been made towards reconstructing Marion Island’s glacial chronology (Rudolph et al., 2020), the spatial extent of these glacial periods remains unknown. Over the last five decades Marion Island’s glacial geomorphology has been mapped during various field campaigns (Nel et al., 2021), but there is a need for a comprehensive and cohesive spatial geodatabase to provide a holistic glacial reconstruction. This paper aims to provide such a glacial geomorphological map and geodatabase, which incorporate existing inventories as well as new knowledge, that can be used in future studies to reconstruct Marion Island’s Quaternary glacial and landscape history.

2. Study area and previous work

Marion Island is one of the volcanic Prince Edward Islands located in the southern Indian Ocean (Figure 1). The island’s volcanic history is dominated by basaltic effusions and explosive events which can be grouped into an older sequence of Pleistocene outflows, otherwise known as the ‘grey’ lava sequence, a younger sequence of Holocene ‘black’ lava outflows, and undated scoria cones (Verwoerd, 1971). The discovery of glacial striations on sub-Antarctic Marion Island during a scientific expedition in 1965 (Verwoerd, 1971) provided the first evidence for former glaciations on the island. As all glacial evidence found since then only occur within the Pleistocene grey lava sequences (Boelhouwers et al., 2008; Hall, 1978; Van Zinderen Bakker, 1973), a period of glaciation is assumed to succeed (all) surficial grey lava outflows, and predate any black lava outflows or scoria eruptions (McDougall, 1971; Van Zinderen Bakker, 1973; Verwoerd, 1971). As such, several geomorphological studies focused on the mapping and relative-age dating of glacial erosional and depositional features found within the grey lava sequences (Boelhouwers et al., 2001; Hall, 1978, 1981; Hedding, 2006, 2008; Sumner et al., 2002). Most maps, however, were only produced in hardcopy form and are of poor resolution due to the limited spatial resolution (quality) of the topographic and remote sensing data. These maps were based on different data sources and mapping approaches but were all dependant on field observations and aerial imagery. In many cases, the aerial imagery was obscured by cloud cover for regions such as the west coast (South Africa, 1988) while field observations were initially limited owing to a lack of field-based research infrastructure and extensive snow cover in the Central Highland (elevations above 750 m a.s.l.) (Langenegger & Verwoerd, 1971). With the advent of Global Positioning Systems (GPS), accessible satellite data and the aid of Geographic Information Systems (GIS), major improvements were made to the geological and geomorphological mapping of the island (e.g. Boelhouwers et al., 2008; Hedding, 2006, 2008). In addition, the areas that could be accessed by field parties expanded over time due to the increase in personnel, infrastructural support and funding (Nel et al., 2021). Climate change also exposed large parts of the Central Highland ‘ice plateau’ previously covered by persistent snow and ice (Sumner et al., 2004). The most comprehensive glacial thematic map and inventory is that of Nel (2001), which was produced from the verification and expansion of previous observations (Hall, 1978, 1980) and mainly covered the eastern side of the island (except for the Central Highland), but was completed without the aid of GPS. Hedding (2006, 2008) produced a more precise map using satellite imagery and GPS, but only focussed on the newly exposed Central Highland. The aim of this paper is thus to provide a comprehensive and cohesive spatial geodatabase of glacial features compiled from existing inventories and new field observations (see Main Map), which are mapped using high-resolution satellite imagery. This geodatabase will assist future studies that aim to reconstruct the spatial and temporal variations in palaeo-ice extent as well as those assessing rates of landscape development in the newly exposed Central Highland.

Figure 1. The location of Marion Island (inset) and the distribution of pre-glacial grey lava surfaces across the island (Rudolph et al., in press). Prominent landmarks, peaks (▴) and demarcation of coastal sectors are indicated, see text for details.

3. Methods

The mapping of glacial features on Marion Island was limited to the island’s grey lava outcrops and deposits. All geomorphological features that have been recorded in prior works were georeferenced and mapped, whilst generating the inventory with new field observations and interpretations from satellite imagery. Field reconnaissance took place during three field campaigns (April/May, 2017-2019; Rudolph, 2020) to verify the interpretations of Marion Island’s glacial geomorphology (see Boelhouwers et al., 2008; Hall et al., 2011; Rudolph et al., 2020 for summaries). These interpretations followed the approaches of other palaeo-climatic and process-origin landscape reconstructions (see Chandler et al., 2018; Hedding et al., 2018). A summary of the spatial data and satellite imagery used in the mapping process is presented in Table 1.

Table 1. A summary of the data types used in the mapping processes with their specifications and creation dates.

Data Type		Resolution / Specifications	Acquisition / Production Date	Source
Satellite Imagery	QuickBird imagery	2 m cell size	27 August 2009	Digital Globe, USA
	WorldView 1	0.5 m cell size	15 May 2011	Digital Globe, USA
	WorldView 2	panchromatic: 0.5 m cell size; multispectral: 1.8 m cell size – true colour with Blue (450-510 nm), Green (510-580 nm), Red (630-690 nm) bands	11 January 2012	Digital Globe, USA
Digital Spatial Data	Digital Surface Model	1 m cell size; 0.7 m vertical accuracy	2019	National Geo-spatial Information Directorate, RSA
	Geology shapefiles	polygons representing the extent of surficial grey lava areas	2020	Rudolph et al., (2020)
	Hillshade raster and drainage lines layer	produced in this study using ArcGIS® Desktop 10.6
	Field observations with GPS point locations		2006	Hedding (2006), unpublished data
Hardcopy Data	Field sketches	contained in theses and publications	1975–1978	Hall (1978, 1980)
	Maps	contained in thesis, dissertations, publications, scientific reports and hardcopy maps	various	Boelhouwers et al. (2008); Hall (1978); Hedding (2006, 2008); Nel (2001); Verwoerd and Langenegger (1968)

3.1. Data and data processing

All the datasets were processed in ArcGIS® Desktop 10.6, using a Transverse Mercator projection (WGS ‘84 datum) with Longitude 37°E as the central meridian. The National Geo-spatial Information Directorate of the South African Department of Rural Development and Land Reform developed a digital surface model (DSM) in 2019 by photogrammetry using Stereo Pléiades imagery (Table 1). This DSM was used to generate a hillshade raster in ArcGIS® using the ‘Hillshade’ tool (with default parameters) (see Figure 2 B). Drainage lines were also generated in ArcGIS® from the DSM using the ‘Hydrology’ tool sets by first generating ‘Fill’, then ‘Flow Direction’ and then ‘Flow Accumulation’ (with a conditional >50 000 parameter) (see Figure 2 B). Satellite imagery from QuickBird (QB), WorldView 1 (WV1) and WorldView 2 (WV2) were imported into the GIS and georeferenced using distinct point intersections on the calculated drainage line layer (see Figure 2 A and B). The higher resolution WV2 panchromatic and multispectral imagery (refer to Table 1) were primarily used during the mapping process, but it only covers approximately 65% of Marion Island (see Figure 2 A and C). For regions not covered by the WV2 imagery, the lower resolution images, QB and WV1 (Table 1), were consulted. The refined geology shapefiles from Rudolph et al. (in press) were used as a demarcation of (pre-glacial) grey lava geology (see Figure 1 and 2 C).

Figure 2. A comparison of the satellite imagery used in the mapping process: (A) the QuickBird (QB), WorldView 1 (WV1) and WorldView 2 (WV2) panchromatic and multispectral imagery. (B) The hillshade derived from the DSM was used to generate drainage lines (B & C) to which the satellite imagery was georeferenced. (C) The imagery, hillshade and DSM were used to identify glacial features within grey lava surfaces and to (D) map the glacial geomorphology of grey lava areas. This is an example of the hummocky terrain at Skua Ridge (refer to Figures 1 and 4).

3.2. Mapping

A summary of all the mapped features, their morphology and the original source data as depicted in the Main Map, is presented in Table 2. Geomorphological features associated with glacial processes that have already been recorded in prior works (e.g. Boelhouwers et al., 2008; Hall, 1978; Hedding, 2006, 2008; Nel, 2001; Verwoerd & Langenegger, 1968) were digitised first, using the calculated hillshade and grey lava geology layer (Rudolph et al., in press) as the primary reference base layers (Figure 2 B and C). Striations were digitised as point features by their approximate position indicated in field sketches or maps (see Hall, 1978; Nel, 2001; Verwoerd & Langenegger, 1968) or from GPS coordinates (Hedding, 2006; Rudolph, 2020). The attribute data of the ‘striations’ layer include author(s), data source (i.e. map or coordinates) and the method of how the original authors determined the striation bearing (e.g. measured by compass, electronic GPS compass or inferred from an orientated arrow on a map or field sketch). Erosional features, e.g. glacial pavement or molded bedrock, and depositional features such as glaciogenic ridges / mounds described by Hall (1978, 1980, 1981) and Boelhouwers et al. (2008) were digitised as polygons using topographical breaks visible on the hillshade layer. Chandler et al. (2018) and Hedding et al. (2018) recommend feature specific investigations to confirm process-form interpretations, especially for depositional features. For the current study, however, existing process-form interpretations (e.g. Boelhouwers et al., 2008; Hall et al., 2011) that attribute glacial processes to the formation of depositional features (e.g. Hall, 1978; 1980; 1981), as opposed to volcanism (e.g. Kent & Gribnitz, 1983), were re-evaluated and are still accepted as correct. The altitudinal limits of the historical persistent snow extent (see Hall, 1978; King, 1954; Verwoerd, 1971; Verwoerd & Langenegger, 1968) and approximate location of the ‘ice plateau’ (see Hedding, 2006; Sumner et al., 2004; Verwoerd, 1971) were also mapped as these have implications for landscape development in the Central Highland.

Table 2. A summary of the features depicted on the Main Map and their morphologies and mapping uncertainties associated with the original data sources or satellite imagery and DSM. This study has expanded on the inventory of all the features described in previous mapping campaigns.

Feature	Morphology	Mapping uncertainties	Previous mapping
Glaciated bedrock	Rock outcrops with evidence of glacial abrasion, polishing and plucking. They vary in relief between 1 m to >20 m, individual features are 1 m to >10 m in length.	Smaller scale abrasion surfaces cannot be identified from imagery. Many pavements are covered in till or vegetation which makes delimiting the extent of glaciated surface from the imagery difficult.	Boelhouwers et al. (2008); Hall (1978); Hedding (2006); Nel (2001)
Striations	Streamlined grooves on bedrock surfaces, from <1 cm to>10 m in length, <1 cm wide and <1 cm deep.	Records pre-2005 do not provide exact locations and not all provide direct orientation measurements.	Hall (1978); Hedding (2006); Nel (2001); Verwoerd and Langenegger (1968)
Glaciogenic sediments	Glacial depositional units at lower altitudes, which consist of clasts of varied shape and size from angular to rounded boulders. These sediments represent either shallow deposits on bedrock, or deposits of >5 m thick.	It is difficult to distinguish between grey lava glacial deposits and adjacent fluvial or colluvial gravel from the satellite imagery alone. Vegetation often covers the boundaries between of these deposits, which makes delimiting them difficult.	Boelhouwers et al. (2008); Hall (1978, 1981); Nel (2001); Sumner et al. (2002)
Glaciogenic mounds and ridges	Distinct elements of positive relief within glacial sediments that can be linear, conical, asymmetrical or crescentic in shape and vary in sizes from <1 m to over 1 km in length.	Erosion, slope processes and vegetation may flatten the topographies or obscure the boundaries of these features making them difficult to identify of the DSM. Patterns in linear-shaped mounds/ridges may have been disrupted by erosional processes	Hall (1978); Nel (2001)
Fabric analysis of glaciogenic material	The results from a detailed fabric analysis of megaclasts are indicated by a line symbol with diamond pointed end, aligned in the generalised direction of the fabric.	The fabric orientation indicated shows the generalised ice-flow direction and is not the estimate for the exact point location.	Hall (1978, 1980)
Moraines	Distinct linear deposits comprising of large (1-3 m) boulders and smaller sub-angular clasts. These are specifically associated with marginal extents of former glaciers. Moraines are found on glaciogenic sediments or near scarp edges of high-lying massifs.	Features previously described and sketched as moraines are not distinct on the imagery and DSM. Moraines which have been disturbed by post-depositional erosion may now be identified as mere glacial sediments/ridges.	Boelhouwers et al. (2008); Hall (1978)
Hummocky terrain	Glacial sediments deposited in chaotic fashion with undulating topography, mounds and kettle lakes. Specifically associated with former ice standstills. Can be coupled with organised moraine sequences.	Push / terminal moraines could potentially appear as mounds due to morphological disruption by outwash or erosion.	Hall (1978, 1980)
Cirques, glacial troughs and scarps	Steep scarps that are associated with glacial erosion. Cirques are crescentic-shaped headwalls and troughs are U-shaped valleys, associated with palaeo-glacial basins.	Scarps may not be attributed to glacial erosion alone, but also to catastrophic landslides or volcanism.	Hedding (2006)
Historical snow limits and the ice plateau	The lower altitudinal limits of summer snow extent, as observed by earlier explorers. The position of ice remnants (‘ice-plateau’) last recorded in the 1960s.	Data is based on snap-shot observations and not precise mapping, and, therefore, may have spatial and temporal inaccuracies.	Hall (1978); Hedding (2006); King (1954); Rand (1954); Sumner et al. (2004); Verwoerd (1971); Verwoerd and Langenegger (1968)
Dilatation outcrops	Rock outcrops with severe dilatation cracking. Genetic origin is unknown as it may be joint or glacial unloading.	On the imagery these outcrops appear like any other grey lava outcrop and relies on field-based observations for verification.	unmapped

4. Glacial geomorphology

A collation of Marion Island’s glacial geomorphological features is shown in the Main Map. Overall, nine categories of glacial geomorphological features have been identified and mapped (Table 2). Features of glacial origin are markedly more abundant on the east coast, possibly because the west coast is more volcanically active (McDougall et al., 2001; Verwoerd, 1971; Verwoerd et al., 1981) and recent (or post-glacial) outflows would bury any evidence of glaciation (Hall et al., 2011), or because the east coast is better explored than the west or south coasts. Erosional features (e.g. striations, glacial bedrock) are generally found in the Central Highland (> 900 m a.s.l.) and mid-altitude slopes (>400 m a.s.l.) of the island (Hall, 1978; Hedding, 2008; Nel, 2001) (see Main Map). Glacial depositional forms (e.g. glaciogenic sediments and mounds, moraines and hummocky terrain) are mostly found along the coastal plains on the east coast (Main Map). The spatial data (i.e. ESRI map layer packages and shapefiles) associated with the Main Map are available as supplementary data.

4.1. Glaciated bedrock and striations

Bedrock surfaces which show evidence of glacial polishing, abrasion or plucking have been classified using a single category, ‘glaciated bedrock’ (Table 2 and Main Map). This category includes prominent rock outcrops, such as the roche moutonnées, and larger plateaus and high-lying massifs such as Tafelberg and Piew Crags, respectively (Figure 3 A-D). In case of smaller features (<10 m) where individual roche moutonnées can be identified (near Truter Peak, Figure 3 E and F), each outcrop was mapped as a single entity. For larger topographic units with several complexes of plucked features and striated surfaces, e.g. Tafelberg, the entire plateau surface is mapped as a single unit (see Main Map and Figure 3 A and G). The striations found on Marion Island vary in size from a few centimetres to metres in length, but are typically no more than 1 cm wide and or 0.5 cm deep (Table 2). They usually occur on flat bedrock pavements and rounded outcrops or roche moutonnées that exhibit other signs of scouring or plucking processes (Figure 3 B, D and G). The orientation of these features indicates former ice-flow direction, which on the island generally radiates coastward from the Central Highland. This is illustrated by the cartographic symbol for striations in the Main Map. Some striated features previously documented e.g. on Katedraalkrans, north of Black Haglet Valley, or near Albatross Lakes (see Hall, 1978), could not be verified during recent field visits (see Rudolph, 2020) and have thus not been included in the map. Erratics are found mostly on the east coast and vary in size from less than a metre to larger than three metres, and commonly occur on some of the glaciated outcrops (Figure 3 C and D). Due to their abundance, however, these features were not explicitly mapped.

Figure 3. Examples of erosional features found on Marion Island. On the Tafelberg complex one can find (A) a glaciated bedrock pavement partly covered with erratics and till material; (B) striations and glacial polishing. (C) A large erratic as found on the glaciated outcrop, Piew Crags, and (D) several scattered erratics (white arrows) on glacially moulded and striated bedrock of Tafelberg. (E and F) Different aspects of the same roche moutonnee on the western side of the island, near Truter Peak (G) Glacial abrasions and plucking on Tafelberg. (F) Katedraalkrans as an example of an outcrop where no striations have been found but it exhibits severe dilatation fracturing. Refer to Figure 1 and the Main Map for place names.

4.2. Glaciogenic sediments, mounds and ridges

Grey lava surfaces at lower altitudes predominantly consist of glaciogenic deposits comprises clast shapes that vary between angular, sub-angular plates to rounded boulders of <1 m to >2 m in size (Boelhouwers et al., 2008; Hall, 1978; Nel, 2001; Sumner et al., 2002). Hall (1978, 1981) initiated an extensive megaclast fabric analysis of coastal deposits (i.e. glaciogenic sediments or tills) (e.g. Skua Ridge, Albatross Lakes) and the general direction of ice flow, as interpreted from this analysis, is indicated on the Main Map. This analysis, however, did not comprise all of the glaciogenic depositional units, for example on Long Ridge, Stony Ridge or Kerguelen Rise. For this reason, a broad classification of ‘glaciogenic sediments’ is used to describe all the depositional elements attributed to a glaciogenic origin (see Table 2 and Main Map). Those sediment deposits that have positive relief profiles but lack a distinct crest which is more commonly associated with moraines, are classified as ‘glaciogenic mounds and ridges’. These ‘mounds and ridges’ vary in shape – some are conical, or asymmetrical, while others are longitudinal or crescent-shaped (Main Map). These features also vary in size from a few metres to over a kilometre long, and from 1 m to over 20 m in height (Table 2). Examples of ridges typically include Kerguelen Rise and Stony Ridge, which are mostly associated with lateral ice margins (Hall et al., 2011; Rudolph, 2020), whereas mounds are commonly found on hummocky terrain, for example on Skua Ridge (Figure 4) or Albatross Lakes (Main Map).

Figure 4. A panorama taken from the hummocky terrain at Skua Ridge, looking towards the interior of the island. Major landmarks and other glaciogenic features, such as mounds, are indicated. Refer to Figure 1 for place names and Figure 2 for an indication of how this region was mapped.

4.3. Moraines

In this paper, ‘moraines’ are strictly defined as depositional elements with distinct positive relief on which large (∼1-3 m) boulders have been deposited and still remain in the landscape today (Table 2). The boulders typically lie in a linear fashion on the crest of glaciogenic sediments, for example on either side of the Watertunnel Valley or on the Feldmark Plateau in-land of Karookop (Figure 5 and Main Map). The mapped moraines also include features found on the top of high-lying massifs such Long Ridge or Grey-headed Ridge (Figure 6 and Main Map). These features are clearly identifiable from the hillshade and satellite imagery and are typically associated the marginal boundaries of palaeo-ice extent (see Figure 5 and 6).

Figure 5. (A) The U-shaped trough of the Watertunnel Valley, looking northwards from the bottom end of the valley. (B) On the Feldmark Plateau, a (terminal) moraine found inland of Karoo Kop is associated with a cirque near Snok (double arrows indicate north). (C) The hillshade and DSM of the Feldmark Plateau and Watertunnel Valley (inset shows the location on an island scale). The perspectives of photos in A and B are indicated by black arrows and the location of the hanging valley near Watertunnel Valley are shown. The mapping symbology used for line symbols on the Main Map is presented. See text for details and Figure 1 for places names.

Figure 6. (A) The hillshade and DSM used for mapping the lower reaches of Long Ridge (inset shows the location on an island scale). (B) The WV2 satellite imagery and the moraines identified on the flanks of Long Ridge. The black arrow indicated the perspective of the photograph in D. (C) The geomorphological mapping symbols used for moraines, glaciogenic sediments and scarp features, here overlain on the hillshade. (D) A field photograph of the moraines on the north western flank of Long Ridge.

4.4. Hummocky terrain

Hummocky terrain describes a glacial geomorphic unit that consists of glaciogenic sediments that are deposited in a chaotic fashion exhibiting an undulating topography with kettle lakes and asymmetrical mounds (Bendle et al., 2017; Singh et al., 2011) (Table 2). On Marion Island, this class includes Skua Ridge and Albatross Lakes, both of which comprise well-vegetated slopes with a positive relief of over 5 m with boulders of various sizes and platy clasts scattered across the ridges and mounds (Figure 4). On Skua Ridge, the ‘disintegration ridges’ and ‘push moraines’ described by Hall (1978, 1980) are difficult to delineate from the high-resolution DSM (Figure 2 B). Similarly, at Albatross Lakes, the hillshade does not distinctly highlight all the terminal moraines identified by Hall (1978). Instead, the DSM and hillshade show a series of mounds and depressions, i.e. hummocky terrain related to former zones of stagnant ice, with a few moraines ridges that may indicate the extent of former ice advance(s) (Bendle et al., 2017; Singh et al., 2011) (see Figure 2 and 4 and the Main Map).

4.5. Cirques, glacial troughs and scarps

Future reconstructions of the island’s glacial history will continue to rely heavily on the remnants of grey lava outcrops, ridges or scarps, which have not (notably) been affected by post-glacial volcanism. It is, therefore, worth mapping the most distinct scarps or cliffs that can be interpreted as cirques, headwalls, sidewalls or glacial troughs in an attempt to reconstruct palae-glacial basins (Table 2). The Watertunnel Valley on the south coast, has a distinct cirque wall and U-shaped valley that can easily be delineated from the DSM and satellite imagery (Figure 5 A and Main Map). Along the eastern flank of the valley (towards the Feldmark Plateau), two (side) valleys can be found which may be considered hanging valleys, since their floors do not meet the main valley floor (Figure 5 C). The scarps of Santa Rosa Valley, Black Haglet Valley (Feldmark Plateau), Piew Crags, Tafelberg and Long Ridge are distinct walls that would have, for example, acted as marginal barriers during glacial periods (Main Map). A few smaller cirques are also delineated in the Central Highland (Hedding, 2008), and one specifically on the south eastern reaches of the Feldmark Plateau below the scoria cone Snok (Boelhouwers et al., 2008) (Figure 5 B and C, Main Map). These features collectively will provide the needed framework to reconstruct glacial basins, determine accumulation areas ratios and investigate the probability of the existence of niche glaciers during interglacial periods (Boelhouwers et al., 2008).

4.6. Dilatation outcrops

Some high-lying grey lava outcrops, e.g. Katedraalkrans, a grey lava sliver in the Basalt Gordyn (∼750 m a.s.l.) and the northern reaches of Feldmark Plateau, exhibit an abundance of fractured bedrock material associated with severe dilatation fracturing (see Figure 3 H). The origin of the material is ascribed to joint unloading, as the outcrops provide no other direct evidence of glacial action (McDougall et al., 2001). Still, glacial unloading is not entirely dismissed as the process-origin (see Hall et al., 2011; Rudolph et al., 2020), but currently these outcrops are mapped as dilatation outcrops (Main Map and Table 2). Evidence such as a block stream documented on the middle section Long Ridge (Sumner & Meiklejohn, 2004) and the size and abundance of well-developed periglacial features on Feldmark Plateau (Boelhouwers et al., 2008; Nel, 2001); have led to the hypothesis that these regions have been ice-free for much longer than the surrounding areas (Rudolph et al., 2020). The interpretation of these ‘ice-free’ areas is supported by the general absence of other glacial landforms as can be seen in the Main Map.

4.7. Historical snow limits and the ‘ice plateau’

The term ‘ice plateau’ was used to refer to an ice cap that was ∼50 m thick in the mid-1950s (King, 1954; Rand, 1954) which today has all but disappeared revealing a relatively small valley basin with an outlet to the north-west (Hedding, 2008; Sumner et al., 2004). Permanent (persistent) snow extended down to 600 m a.s.l. at the time of the first scientific surveys (King, 1954; Verwoerd & Langenegger, 1968) and had retreated to above 950 m a.s.l. by 1970 (Hall, 1980; Verwoerd, 1971). The ‘ice plateau’ was traditionally interpreted to be the remnants of the Last Glacial Maximum, ∼ 20 000 years ago (Verwoerd, 1971), however, new evidence suggests a much earlier deglaciation (>35 000 years ago) for the island (Rudolph et al., 2020). Still, historical snow and ice limits are important considerations for Martion Island’s more recent landscape development, as is shown quite clearly by the remarkable absence of periglacial fetaures in the Central Highland above 950 m a.s.l. (Hedding, 2008; Sumner et al., 2004). Understanding the island’s response to contemporary climate change will serve as a baseline for interpreting landscape-climate interactions, such as equilibrium line altitudes and ablation rates througout the Quaternary.

5. Conclusion

The glacial geomorphology of Marion Island is mapped from high-resolution satellite imagery onto a digital surface model (DSM) with a 1 × 1 m cell resolution. Satellite imagery was used to digitise and georeference existing records of the island’s glacial geomorphology, as well as map new glacial evidence found within the island’s grey lava sequences. Nine categories of landforms are mapped, which includes glacial depositional and erosional features, historical snow limits and the extent of the former ‘ice plateau’ as well as regions associated with dilatation fracturing. For future glacial reconstructive studies, the depositional features found predominantly on the east coast can be used to interpret the terminal and lateral extent of palaeo-ice extent. Whereas erosional features and till fabric analysis will assist in interpretations of past glacial flow directions. Other features such as scarps or cirques and ice-free regions will especially aid future studies to reconstruct palaeo-glacial basins or to model accumulation area ratios. In conjunction with this, mapping historical snow limits can allow for a better understanding of landscape-climate interactions and aid in modelling past equilibrium line altitudes or ablation potential. The limited spatial extent of (pre-glacial) grey lava surfaces that remain exposed on the south- and north-west coast, pose a significant limitation for mapping, but the inclusion of periglacial features to future mapping campaigns will aid in a holistic reconstruction of Marion Island’s Quaternary landscape evolution.

Data

The authors have supplied the data used in the production of the accompanying map as ESRI layer-package files.

Software

The mapping and image processing have been completed using ESRI ArcGIS Desktop 10.6.

Acknowledgements

The authors would like to thank the South African National Antarctic Programme and the Department of Environmental Affairs / Environment, Forestry and Fisheries for their logistical support, and the South African National Research Foundation for financial support throughout this study.

Disclosure statement

No potential conflict of interest was reported by the author(s).

Additional information

Funding

This work was supported by the South African National Research Foundation under Grant [SANAP-NRF: 129235].