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Crevasse density, orientation and temporal variability at Narsap Sermia, Greenland

Published online by Cambridge University Press:  29 March 2023

Maximillian Van Wyk de Vries Open the ORCID record for Maximillian Van Wyk de Vries [Opens in a new window] ,
James M. Lea  and
David W. Ashmore Open the ORCID record for David W. Ashmore [Opens in a new window]
Maximillian Van Wyk de Vries*
Affiliation:
Department of Geography and Planning, University of Liverpool, Liverpool L69 7ZT, UK School of Geography and the Environment, University of Oxford, Oxford OX1 3QY, UK
James M. Lea
Affiliation:
Department of Geography and Planning, University of Liverpool, Liverpool L69 7ZT, UK
David W. Ashmore
Affiliation:
Department of Geography and Planning, University of Liverpool, Liverpool L69 7ZT, UK
*
Author for correspondence: Maximillian Van Wyk de Vries, E-mail: [email protected]
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Abstract

Mass loss from iceberg calving at marine-terminating glaciers is one of the largest and most poorly constrained contributors to sea-level rise. However, our understanding of the processes controlling ice fracturing and crevasse evolution is incomplete. Here, we use Gabor filter banks to automatically map crevasse density and orientation through time on a ~150 km2 terminus region of Narsap Sermia, an outlet glacier of the southwest Greenland ice sheet. We find that Narsap Sermia is dominated by transverse (flow-perpendicular) crevasses near the ice front and longitudinal (flow-aligned) crevasses across its central region. Measured crevasse orientation varies on sub-annual timescales by more than 45$^\circ$ in response to seasonal velocity changes, and also on multi-annual timescales in response to broader dynamic changes and glacier retreat. Our results show a gradual up-glacier propagation of the zone of flow-transverse crevassing coincident with frontal retreat and acceleration occurring in 2020/21, in addition to sub-annual crevasse changes primarily in transition zones between longitudinal to transverse crevasse orientation. This provides new insight into the dynamics of crevassing at large marine-terminating glaciers and a potential approach for the rapid identification of glacier dynamic change from a single pair of satellite images.

Keywords

Crevassesglacier flowremote sensing
Type
Article
Information
Journal of Glaciology , Volume 69 , Issue 277 , October 2023 , pp. 1125 - 1137
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Creative Commons
Creative Common License - CCCreative Common License - BY
This is an Open Access article, distributed under the terms of the Creative Commons Attribution licence (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted re-use, distribution and reproduction, provided the original article is properly cited.
Copyright
Copyright © The Author(s), 2023. Published by Cambridge University Press on behalf of The International Glaciological Society

1. Introduction

The future response of the Greenland and Antarctic ice sheets to changing climatic conditions remains one of the most uncertain factors in forecasts of future sea-level rise (Nowicki and others, Reference Nowicki2016; Pörtner and others, Reference Pörtner2019; Goelzer and others, Reference Goelzer2020; Masson-Delmotte and others, Reference Masson-Delmotte2021). The majority of the mass loss of these ice sheets occurs at marine-terminating glaciers, which lose mass in part by calving icebergs directly into the ocean (Benn and others, Reference Benn, Hulton and Mottram2007; Vieli and Nick, Reference Vieli and Nick2011). Changes in the frontal conditions of marine-terminating glaciers can drive rapid glacier retreat (Venteris, Reference Venteris1999; Nick and others, Reference Nick, Vieli, Howat and Joughin2009; Kochtitzky and Copland, Reference Kochtitzky and Copland2022), and can promote rapid ice thinning far from the ice front due to dynamic glacier changes (e.g. Pritchard and others, Reference Pritchard, Arthern, Vaughan and Edwards2009).

Understanding the retreat rates of marine-terminating glaciers relies on identifying the glacier dynamic conditions. Glacier dynamic conditions and changes are currently assessed primarily based on ice velocity calculated using feature tracking, which relies on the existence of coherent satellite image pairs with a suitably low temporal baseline. In the case of marine-terminating glaciers, conditions in fast-flowing regions and close to the calving front often cannot be resolved due to decorrelation or calving ice losses between the two images. The region immediately up-glacier of the ice front is critical for our understanding of calving processes, so in this study, we develop a method for the identification of glacier crevasse patterns from a single image.

Mass loss at marine-terminating glaciers occurs partly through iceberg calving, as fractures propagate through the entire thickness of the glacier. Glacier flow continuously delivers new ice from inland to the glacier front. A glacier's terminus position is stable if the rate of frontal ablation is approximately equal to the flux of ice to the front, and retreating if the rate of frontal ablation exceeds the ice flux. Iceberg calving can drive rapid frontal ablation and glacier retreat (102–103 m a−1), particularly where glaciers terminate in deep water (Venteris, Reference Venteris1999; Rivera and others, Reference Rivera, Corripio, Bravo and Cisternas2012; Bondzio and others, Reference Bondzio, Morlighem, Seroussi, Wood and Mouginot2018; Moffat and others, Reference Moffat2018). In order for an iceberg to calve, a fracture must penetrate through the entire ice thickness and separate one or many pieces of ice from the rest of the glacier. These fractures are known as crevasses and are widely present in glacial environments.

Cracks form due to tensile or shear stresses in the ice which locally exceed its strength, and may evolve into crevasses (Fig. 1). Crevasses are present on glaciers across a wide range of scales, from metre scale fractures in valley and cirque glaciers to rifts tens of kilometres long at the margins of the Antarctic ice sheet. Crevasses are thought to form approximately perpendicular to the principal normal stress direction: transverse or flow-perpendicular crevasses (oriented ~90$^\circ$ from the direction of ice flow; mode 1) are commonly found in zones of longitudinal extension, while longitudinal or splaying crevasses (oriented approximately parallel to the direction of ice flow; mode 2) are commonly found in zones of longitudinal compression (Fig. 2). Lateral shear at the margins of a glacier often results in crevasses oriented ~45$^\circ$ from the valley walls (Nye, Reference Nye1952; Glen and Perutz, Reference Glen and Perutz1955; Nye, Reference Nye1955; Hudleston, Reference Hudleston2015; Colgan and others, Reference Colgan2016; Jennings and Hambrey, Reference Jennings and Hambrey2021). Creep closure usually limits crevasse depth to a few tens of metres, and understanding the conditions under which crevasses may propagate through the entire ice column is key to evaluating the drivers of iceberg calving (Nye and Mott, Reference Nye and Mott1953; Nye and Perutz, Reference Nye and Perutz1957; Benn and others, Reference Benn, Hulton and Mottram2007; Mottram and Benn, Reference Mottram and Benn2009).

Fig. 1. Diagram describing the main categories of crevasses, and their formation mechanisms.

Fig. 2. Location of Narsap Sermia in Greenland and within Nuup Kangerlua, and view of the glacier from Sentinel-2.

A number of analytical and numerical approaches have been used to evaluate the influence of crevassing on glacier calving, from simple ‘zero-dimensional’ calving laws to full 3-D glacier models (e.g. Nye and Perutz, Reference Nye and Perutz1957; van der Veen, Reference van der Veen1998; Pralong and Funk, Reference Pralong and Funk2005; Mottram and Benn, Reference Mottram and Benn2009; Krug and others, Reference Krug, Weiss, Gagliardini and Durand2014; Choi and others, Reference Choi, Morlighem, Wood and Bondzio2018; Todd and others, Reference Todd2018; Bassis and others, Reference Bassis, Berg, Crawford and Benn2021; Crawford and others, Reference Crawford2021; Cook and others, Reference Cook, Christoffersen and Todd2022). Certain early studies of calving bypass crevasses entirely, and relate glacier calving rate to the water depth at the ice front (Brown and others, Reference Brown, Meier and Post1982; van der Veen, Reference van der Veen1998) or ice front height (Pfeffer and others, Reference Pfeffer1997). These empirical formulations allow models to reproduce observed rates of ice retreat in some cases but are not physically based. More recent studies have proposed different calving models related to ice dynamics and physical variables, for instance, height-above-buoyancy models (Vieli and others, Reference Vieli, Funk and Blatter2001), crevasse depth criteria (Benn and others, Reference Benn, Hulton and Mottram2007), von Mises tensile stress criteria (Morlighem and others, Reference Morlighem2016; Choi and others, Reference Choi, Morlighem, Wood and Bondzio2018), kinematic calving laws (Levermann and others, Reference Levermann2012) and linear elastic fracture mechanics approaches (Yu and others, Reference Yu, Rignot, Morlighem and Seroussi2017). Crevasses are commonly parameterized in numerical models as damage fields, accounting for the bulk effect of brittle fractures on viscous ice flow (Pralong and others, Reference Pralong, Funk and Lüthi2003; Pralong and Funk, Reference Pralong and Funk2005; Borstad and others, Reference Borstad2012; Lhermitte and others, Reference Lhermitte2020). Advances in computational power have also enabled the use of discrete element models to simulate crevasse calving, which can reproduce individual calving events in greater detail (Bassis and others, Reference Benn2017; Cook and others, Reference Cook2018; Gong and others, Reference Gong2018; van Dongen and others, Reference van Dongen2020). Many advances in the numerical description of crevasses have been made over the past 20 years, but limitations remain in our understanding and numerical representation of crevasse penetration at the ice front, and ice-sheet models lack a universally applicable and computationally efficient representation of calving. Large-scale observations of crevasse evolution are therefore key to developing and evaluating new crevasse models.

Crevasses form visible traces on the surface of glaciers, and can therefore be identified and monitored remotely via ground, air or satellite-based imagery. Manual identification of crevasses in remotely sensed imagery dates back to almost 50 years (e.g. Krimmel and Meier, Reference Krimmel and Meier1975), and has been reviewed by Colgan and others (Reference Colgan2016) and Jennings and Hambrey (Reference Jennings and Hambrey2021). The study of glacier surface crevasse patterns is a key method in structural glaciology and can yield insight into glacier strain history, current dynamics and future stability. Structural glaciology is a sub-discipline that aims to evaluate glacier processes using their structural characteristics: crevasses, faults, folds, foliation and more (Hudleston, Reference Hudleston2015; Jennings and Hambrey, Reference Jennings and Hambrey2021). For instance, crevasses were manually mapped at Worthington Glacier, USA (Harper and others, Reference Harper, Humphrey and Pfeffer1998), Haut Glacier d'Arolla, Switzerland (Goodsell and others, Reference Goodsell, Hambrey, Glasser, Nienow and Mair2005), Kvíárjökull, Svínafellsjökull and Fjallsjökull, Iceland (Phillips and others, Reference Phillips2017; Swift and others, Reference Swift2018; Dell and others, Reference Dell, Carr, Phillips and Russell2019, respectively), Isunguata Sermia, Greenland (Jones and others, Reference Jones, Ryan, Holt and Hubbard2018) and Fountain Glacier, Canada (Jennings and others, Reference Jennings, Hambrey, Moorman, Holt and Glasser2022).

Semi-automated crevasse mapping methods are also used, including the use of histogram equalization or edge enhancement image processing to facilitate manual crevasse identification (Colgan and others, Reference Colgan2011, Reference Colgan2016). However, manual or semi-automated crevasse identification is both subjective and time-consuming, preventing multi-temporal mapping of crevasses over large spatial areas. Therefore, a range of fully automated crevasse mapping techniques have also been developed: Bhardwaj and others (Reference Bhardwaj, Sam, Singh and Kumar2016) used a simple Landsat band ratio technique to map small crevasses on Shaune Garang glacier (Himalaya), Gong and others (Reference Gong2018) used the Radon transform to evaluate linear features on a surging outlet of Austfonna (Svalbard), Chudley and others (Reference Chudley2021) compared a Random Forest classification to crevasse maps from high-resolution elevation data in Greenland, Christmann and others (Reference Christmann2021) compared DEM-derived and manually mapped crevasse fields over Greenland to stress change maps, Lai and others (Reference Lai2020) used a neural network to identify Antarctica-wide rifts using MODIS Mosaic of Antarctica imagery, Zhao and others (Reference Zhao, Liang, Li, Duan and Liang2022) applied deep learning to Sentinel-1 radar imagery to map fractures in Antarctic ice shelves, and Izeboud and Lhermitte (Reference Izeboud and Lhermitte2023) develop a method for automated crevasse detection using a normalized radon transform. Despite the recent advances in automated crevasse mapping, most existing techniques either require an extensive training dataset (e.g. machine learning-based methods; Lai and others, Reference Lai2020; Chudley and others, Reference Chudley2021; Zhao and others, Reference Zhao, Liang, Li, Duan and Liang2022), or only provide overview statistics instead of the location and attributes of individual crevasses (e.g. Radon transform-based methods; Gong and others, Reference Gong2018).

Here, we describe a new automated crevasse mapping method based on processing images with linear feature detection kernels: Gabor filters. This method is computationally fast, does not require any training data and provides a map of individual crevasse locations. We apply this method to automatically map the occurrence of crevasses on 6 years of Sentinel-2 data (224 images) on a ~150 km2 region of Narsap Sermia, an outlet glacier of the Greenlandice sheet. We also calculate glacier velocity maps so as to compare crevasse fields to glacier velocity magnitude and direction. We use these data to explore the following three research questions:

  1. 1. What is the spatial pattern and orientation of crevasses across a marine-terminating glacier?

  2. 2. Is the distribution, extent and orientation of crevasses constant through time, or does it exhibit seasonal and/or multiannual changes?

  3. 3. What is the relation between crevasse characteristics and glacier velocity?

2. Study area

Narsap Sermia is an outlet glacier draining the southwest margin of the Greenland ice sheet, and the closest marine-terminating glacier to Greenland's capital and most populous city, Nuuk (Pearce and others, Reference Pearce2018). Alongside Kangiata Nunaata Sermia and Akullerssuup Sermia, Narsap Sermia calves icebergs directly into Nuup Kangerlua (Nuuk Fjord), which can be advected down-fjord and have the potential to impede shipping routes to Nuuk. The frontal position of Narsap Sermia remained close to its Little Ice Age position until the early 21st century (Motyka and others, Reference Motyka2017), whereupon it has exhibited several episodes of rapid ice retreat (Motyka and others, Reference Motyka2017; Davison and others, Reference Davison2020), the latest of which is ongoing today. Narsap Sermia currently terminates in moderate to shallow depth water (~200 m; Morlighem and others, Reference Morlighem, Rignot, Mouginot, Seroussi and Larour2014), but a deep subglacial trough is present ~5–20 km up-glacier from the 2022 calving front (Morlighem and others, Reference Morlighem, Rignot, Mouginot, Seroussi and Larour2014; Motyka and others, Reference Motyka2017). If Narsap Sermia's calving front were to reach the retrograde slope at the down-glacier edge of this subglacial trough, it could enter a phase of runaway retreat observed at other marine-terminating glaciers (Venteris, Reference Venteris1999; Motyka and others, Reference Motyka2017). This runaway retreat might also be associated with changes in calving style, affecting the quantity and size distribution of icebergs advected towards Nuuk. Narsap Sermia has three subsidiary ice fronts terminating in ice-marginal lakes, including the ~20 km2 glacial lake Iluliartôq. All three lakes have varying volumes and drain under the glacier, with the lowermost lake remaining fully drained since the latest episode of frontal retreat (post-2014). The societal importance of calving processes at Narsap Sermia, along with its high degree of crevassing and ongoing frontal retreat, make it an ideal case study for spatiotemporal changes in crevassing.

3. Methods

We implement a method to automatically detect and calculate the orientation of crevasses within satellite images using a Gabor filter bank. A Gabor filter is composed of a sinusoidally modulated Gaussian kernel and is sensitive to image texture. By combining a bank of filters of different orientations, we extract individual crevasse locations and orientations from optical satellite images (Fig. 3). We describe the attributes of the Gabor filter bank and crevasse detection in more detail in Appendix A1. This method is computationally rapid, extracts individual crevasse orientations and does not require a training dataset. We apply this method, which we term the Gabor crevasse detector (GCD), to all 10 m resolution near-infrared (band 8) Sentinel-2 L1C images of Narsap Sermia from its operational start in June 2015 to April 2022. We select the near-infrared band as it shows a strong contrast between crevassed and non-crevassed areas, but do not expect major differences if computed with other visible spectrum bands or band combinations. We exclude all images in which the glacier is obscured by cloud cover or shadows, retaining the 224 images in which the entire glacier area of interest is unobstructed. As well as calculating a binary crevasse mask and crevasse orientation map for each image, we calculate three crevasse statistics in 20 × 20 pixel sub-regions. The three statistics are crevasse spatial density (the ratio of pixels classified as crevasses to the total number of pixels in the sub-region), the median crevasse orientation and the mean absolute deviation of the measured crevasse orientation. The mean absolute deviation provides an estimate of the local degree of dispersion of measured crevasse orientations. We evaluate the GCD in Appendix A3 by comparing it to two other, previously used crevasse mapping techniques: digital elevation model (DEM) thresholding and manual delineation.

Fig. 3. Diagram of the main steps involved in the automated crevasse mapping method. A time series of satellite imagery is convolved with a Gabor filter bank, creating maximum Gabor phase and maximum response angle maps. The maximum Gabor phase map is then thresholded to extract a crevasse network, with the orientation of each crevasse obtained from the maximum response angle map.

We use feature-tracking toolbox GIV to calculate 80 m-resolution glacier-surface-velocity and strain maps for Narsap Sermia, using a frequency-domain multi-pass image correlator (Van Wyk de Vries and Wickert, Reference Van Wyk de Vries and Wickert2021). We use velocity maps to assess glacier surface strain rates, and the orientation of crevasses relative to ice flow direction. We also calculate apparent displacements over the surrounding bedrock to correct for georeferencing errors and evaluate local noise levels. We compile three different datasets of image pairs based on the temporal separation between images: short period (1–8 d), medium period (9–90 d) and long period (300–430 and 650–800 d). This separation allows us to monitor displacements over both regions of fast ice flow in which surface decorrelation occurs rapidly and regions of slow ice flow in which long temporal separation is necessary for resolvable displacement to occur.

We calculate velocities from a total of 7194 image pairs, of which 330 are short-period image pairs, 2306 are medium-period image pairs and 4558 are long-period image pairs. Calculating a large number of individual velocity maps improves the precision of median velocity maps (Millan and others, Reference Millan2019; Van Wyk de Vries and Wickert, Reference Van Wyk de Vries and Wickert2021). A full description of our velocity mapping workflow is provided in Appendix A2. We average all processed velocity maps into a median velocity map covering the entire 6 year period. We also calculate annual median velocity maps for each of the three image temporal separations (short, medium and long). We calculate longitudinal (σ xx), transverse (σ yy) and shear (σ xy) strain rate maps from each of the overall and annual median velocity maps. Finally, we calculate the relative angle between measured crevasse orientation (calculated using the GCD described above) and local ice-flow direction and classify crevasses into three categories: longitudinal crevasses oriented close to (0–33$^\circ$) of the direction of ice flow, transverse crevasses oriented approximately perpendicular to the direction of ice flow (66–90$^\circ$) and crevasses oriented in neither of these directions (33–66$^\circ$).

4. Results

We find an overall decrease in measured crevasse density with distance away from the calving front at Narsap Sermia, with three main styles of crevassing (Fig. 4). The first type of crevasse, oriented approximately perpendicular to the direction of ice flow, is abundant within 5 km of the glacier marine calving front and to a lesser degree at subsidiary lacustrine calving fronts. These crevasses form large, arcuate fractures in the extensively damaged zone proximal to the calving front. The second type of crevasses, oriented ~45 $^\circ$ from the direction of ice flow, are most abundant on the flanks of the zone of fast ice flow at the centre of the valley. The third type, oriented approximately parallel to the direction of ice flow, is primarily located within the centre of the glacier valley. A 3 km long by 1 km wide region located halfway up the outlet glacier (~10 km from the ice front) is dominated by this third, longitudinal crevasse type. While the first, transverse, crevasse type is the most abundant close to the ice front, the second and third crevasse types are also present to a lesser degree.

Fig. 4. Measured crevasse orientation map of Narsap Sermia from 17 April 2022, with inset showing the two key crevasse zones: a zone of transverse crevassing near the ice front, and a zone of longitudinal crevassing up-glacier of this. The polar histograms show the angle between the direction of crevassing and the direction of ice flow in each inset.

We assess crevasse and velocity changes at three 1 km2 zones on the glacier representing these main regions: the first ‘down-glacier’ zone is located close to the ice front in the zone of longitudinal crevassing (Fig. 5), the second ‘transitional’ zone is located 7.5 km up-glacier at the transition between the longitudinal crevassing and transverse crevassing zones (Fig. 6) and the third ‘up-glacier’ zone is located within the zone of transverse crevassing (Fig. 7). The down-glacier zone is located in a region of moderate depth-to-bedrock (~250 m ice thickness; BedMachine v4.0), low slope subglacial topography while the transitional zone is on the downstream tip of a subglacial ridge and the up-glacier zone is at the centre of the same subglacial ridge and close to its transition into a subglacial trough (Fig. 8e).

Fig. 5. Time series of measured crevasse density (b), measured crevasse orientation relative to the direction of ice flow (c) and ice velocity (d) for the 1 km2 down-glacier zone at the front of Narsap Sermia (a). The dark line represents the median monthly velocity. Note that the y-axes are different to Figs 6 and 7 to highlight the seasonal variation in each location.

Fig. 6. Time series of measured crevasse density (b), measured crevasse orientation relative to the direction of ice flow (c) and ice velocity (d) for the 1 km2 transitional zone ~5 km up-glacier from the front of Narsap Sermia (a). The dark line represents the median monthly velocity. Note that the y-axes are different to Figs 5 and 7 to highlight the seasonal variation in each location.

Fig. 7. Time series of measured crevasse density (b), measured crevasse orientation relative to the direction of ice flow (c) and ice velocity (d) for the 1 km2 up-glacier zone ~10 km up-glacier from the front of Narsap Sermia (a). The dark line represents the median monthly velocity. Note that the y-axes are different from Figs 5 and 6 to highlight the seasonal variation in each location.

Fig. 8. Median ice flow speed (a), effective strain rate (b), measured crevasse orientation seasonality (c), crevasse density seasonality (d) and subglacial topography (e). Measured crevasse orientation and density seasonality are calculated as the average of September 2020 to May 2021 minus the average of June 2020 to July 2020. Note that the apparently large seasonal changes on the southern lake-terminating glacier are highly uncertain, and we do not interpret these. Subglacial topography is obtained from BedMachine v4.0 and is referenced to the local mean sea level (geoid).

Crevasses also exhibit seasonal variability, with strong seasonal changes in both the intensity and dominant orientation of crevasses in some regions of Narsap Sermia. Measured crevasse density remains high throughout the year in the down-glacier zone, with close to 100% crevasse coverage throughout the year (Fig. 5a). The intensity of secondary (45$^\circ$ and longitudinal) crevassing exhibits minor variability, although transverse crevassing remains dominant at all times. The median angle between measured crevasse orientation and ice flow in the down-glacier zone varies between 55$^\circ$ and 75$^\circ$ (Fig. 5b). Seasonal variability in both measured crevasse density and orientation is high at the transitional zone, with a summer minimum in the degree of crevassing (Fig. 6a). Measured crevasse density reaches close to 100% in the winter and spring, but declines to <50% in the mid-summer (Fig. 6b). The degree of summer (July) crevassing in the transitional zone has increased from $\sim \!45\percnt$ in 2016 to $\sim \!60\percnt$ in 2021. The median angle between measured crevasse orientation and ice flow in this zone fluctuates from ~20$^\circ$ in the summer to 70$^\circ$ in late autumn to spring (Fig. 6b). In the up-glacier zone the median angle between measured crevasse orientation and ice flow remains low (10–20$^\circ$) and the intensity of crevassing remains close to 100% throughout the year (Figs 7a, b).

Ice velocities show a similar trend in all three of these zones, with a seasonal minima in the late summer and maxima in the early spring (Figs 5c, 6c, 7c). Velocities also show a long-term acceleration, with 2021 velocities being ~33% higher than in 2016. In the transitional zone, the yearly velocity maxima coincide with the yearly minima in measured crevasse density and angle between measured crevasse orientation and ice flow (Fig. 6).

The region of high seasonal variation in measured crevasse orientation is spatially limited to the boundary between the frontal region of transverse crevasses and the up-glacier zone of longitudinal crevasses. This region exhibits a $> \!20^\circ$ variation in median angle between measured crevasse orientation and ice flow throughout the year (Fig. 8c). A broader region exhibits a moderate to high seasonal variation in measured crevasse density, with the surroundings of the up-glacier zone of longitudinal crevasses all exhibiting a ~20% seasonal variation in measured crevasse density (Fig. 8d). The up-glacier zone of longitudinal crevassing is located above a subglacial ridge (Fig. 8e) and in an area with very low velocity gradients and effective strain rates (Figs 8a, b).

5. Discussion

5.1 Key findings and limitations

Our automatically processed crevasse orientation maps, based on 6 years of Sentinel-2 data and 224 individual images of Narsap Sermia, provide the first dense time series of changes crevasse change at a major glacier. We first show that the large-scale pattern of crevassing remains consistent across the entire study period, with a zone of longitudinal crevassing near the glacier front and a zone of transverse crevassing up-glacier of this. These persistent large-scale crevasse patterns likely relate to the glacier geometry and bed elevation. Conversely, we identify both strong seasonal and multiannual variability when examining the time series of measured crevasse density (the spatial density of crevasses in a given area) and orientation (the median difference between crevasse angle and ice-flow direction). The main glacier trunk exhibits a seasonal minimum in the degree of crevassing in the late summer, and some regions exhibit a seasonal fluctuation between transverse crevassing (high angle to ice-flow direction) to longitudinal crevassing (low angle to ice-flow direction). Velocity mapping highlights a multiannual increase in ice flow speeds with the greatest increase close to the ice front (Figs 5d, 6d, 7d), which is a possible cause for observed multi-annual increases in measured crevasse density and changes in measured crevasse orientation 5–10 km up-glacier from the ice front.

Our GCD crevasse mapping method can be leveraged to rapidly map the characteristics of thousands of individual crevasses or whole crevasse fields. Using automated instead of manual crevasse mapping methods can enable structural glaciology techniques to be upscaled from single glaciers and time periods to whole ice caps and/or multiple time periods. Our results from Narsap Sermia show that a crevasse map derived from a single time period might not be representative of the glacier's overall conditions. The first implication of this finding is that glacier structure may be more dynamic than previously considered (Hudleston, Reference Hudleston2015; Jennings and Hambrey, Reference Jennings and Hambrey2021), and be a valuable tool for assessing short-timescale glacier change. The second implication is methodological: studies aiming to use crevasses to map a glacier's dynamic conditions must account for this temporal variability, as manually mapping crevasses over a single time step may produce a map reflecting transient conditions at this point in time, rather than the longer timescale forcings of interest (e.g. Phillips and others, Reference Phillips2017; Jones and others, Reference Jones, Ryan, Holt and Hubbard2018; Swift and others, Reference Swift2018; Dell and others, Reference Dell, Carr, Phillips and Russell2019; Jennings and others, Reference Jennings, Hambrey, Moorman, Holt and Glasser2022).

While the GCD described in this study has a number of advantages, it also has certain limitations. An ideal crevasse model would be able to delineate all crevasses in a glacier, regardless of their scale or physical appearance, while also not falsely classifying any other glacier surface features as crevasses. The complex and highly variable nature of a glacier surface makes this a complex task: glaciers can exhibit a wide range of surface expressions (e.g. Herzfeld and others, Reference Herzfeld, Clarke, Mayer and Greve2004; Colgan and others, Reference Colgan2016) and features other than crevasses can form linear expressions on a glacier surface, including medial moraines, longitudinal foliation, ogives and flow banding (Hudleston, Reference Hudleston2015; Jones and others, Reference Jones, Ryan, Holt and Hubbard2018; Jennings and Hambrey, Reference Jennings and Hambrey2021). The GCD is in most cases unable to distinguish between linear expressions on the ice surface related to crevassing and those related to other processes. The GCD can identify sub-pixel resolution crevasses (<10 m in the case of Sentinel-2), but requires them to leave distinct surface expressions, and will likely fail where multiple small crevasses are present within a single pixel. The GCD only identifies a single-dominant crevasse orientation at any given pixel, which can result in information loss at pixels where two or more crevasses of different orientations intersect. Finally, the GCD requires a surface expression of crevasses in optical imagery, and will fail to identify crevasses entirely buried by snow (which can be identified using other methods; e.g. Eder and others, Reference Eder, Reidler, Mayer and Leopold2008; Thompson and others, Reference Thompson2020). The use of SAR data could enable crevasse detection in cases where it is not possible in optical data, but we limit our use of the GCD to optical data in this study. Crevasse surface expression and degree of shadowing can also be affected by sun azimuth. We, therefore, suggest that the GCD be primarily used in areas where (1) crevasses are close to or greater than the resolution of the imagery used to map them, (2) crevasses are the dominant structural feature on the glacier surface and (3) the glacier surface is largely free of snow cover.

5.2 Drivers of seasonal cycle

The seasonal variation in crevasse characteristics observed (density and orientation) could be an artefact of other seasonal changes, such as a seasonal change in snow cover or illumination. We critically evaluate the possibility of each of these in this section and discuss why we think the observed seasonal variation on the main branch of Narsap Sermia represents a real signal. Illumination: At a latitude of more than 64° N, Narsap Sermia is subject to a strong seasonal cycle in illumination. This could plausibly cause an apparent seasonal cycle in crevassing by reducing the winter illumination and modifying illumination angles throughout the year. We plot the seasonal change in midday sun azimuth (variation between 198° and 213°) and midday sun elevation (variation between 2° and 46°) alongside the seasonal change in crevassing in the transitional zone in Supplementary Section S2, with the two being anti-correlated. However, with the exception of shadowed areas, we would expect the effect of illumination to be approximately constant across the glacier for crevasses of a given orientation. Our seasonal variability results are not consistent with a change in illumination alone, as both the seasonality in measured crevasse density and orientation are spatially variable across the glacier (Fig. 8). The seasonal variation in crevasse cover and orientation is much higher in the transitional zone than in the up-glacier or down-glacier zones (Figs 5–7). In addition, we manually excluded all winter imagery in which the surface of the glacier is covered by shadows or poorly illuminated, so direct shadowing cannot be a contributor to our observed seasonality.

Snow cover: With winter temperatures below freezing and summer temperatures above freezing, Narsap Sermia experiences a seasonal cycle in snow cover. Snow can cover the glacier surface and mask crevasses, or even preferentially cover crevasses of a certain orientation due to a prevailing wind direction (katabatic winds) or differing crevasse sizes. Snow may also cause an apparent spatial gradient in this seasonal variation, with more snowfall and masking of crevasses for a longer duration at higher altitudes. However, we find it unlikely that snow could explain the apparent pattern of crevasse changes as: (1) at Narsap Sermia, crevasses are large enough to never be fully snow-covered. Crevasses are fully visible even in images from mid-winter. (2) We would expect snow to reduce the apparent crevasse density in the accumulation season and reduce it in the ablation season, but the area with the highest seasonal variation in measured crevasse density reaches a minimum during the ablation season (Fig. 6). (3) We expect the effect of snow cover to be either uniform across the glacier or elevation dependant, whereas the observed pattern of seasonal changes is more complex.

Snow cover may be a factor in the marginal areas of Narsap Sermia (e.g. southern lake-terminating branch), which exhibit much slower flow velocities, smaller crevasses and have an apparent summer maximum in crevassing. However, we consider it unlikely that changes in snow cover are a major influence of the observed seasonal cycle in crevassing along the main branch of Narsap Sermia.

We do not consider it likely that artefacts related to seasonal changes in illumination or snow cover are the primary cause of the observed seasonal cycle in measured crevasse density or orientation along the main branch of Narsap Sermia. We also note that the magnitude of this seasonal change is small across most of the glacier ($< \!10\percnt$ at points 1 and 3; Figs 5, 7) and would likely not be apparent from visual interpretation of satellite imagery alone. Seasonal changes in measured crevasse orientation and density are large in the vicinity of point 2, which is located at the transition zone between longitudinal and transverse crevassing. We show a year's worth of imagery at this point in Supplementary Section S1, which clearly shows that the glacier surface is not shadowed or snow-covered throughout the period.

We hypothesize that this cycle is caused by a seasonal shift in the position at which the transverse crevasses begin to open, with them opening further up-glacier in the glacier in the winter (high measured crevasse density, high crevasse angle to flow direction) than in the summer (lower measured crevasse density, low measured crevasse orientation). This mechanism for seasonal variation in crevassing does not require the closing of crevasses over the course of a season: from the Lagrangian reference frame (advected with ice flow), individual crevasses simply open at different times throughout the year. In the Eulerian reference frame (fixed geographic location) this difference can manifest as a seasonal cycle in crevasse density and orientation as different populations of crevasses are advected past the point. This cycle is consistent with the ice velocity trends, with a summer slowdown apparent across the glacier front (Figs 5, 6, 7d). In the absence of dense time series of crevasse density or orientation at other glaciers, it remains unknown whether such zones of high seasonal variability are widespread at tidewater glaciers.

5.3 Crevasses and terminus stability

Our results are not consistent with a binary classification of crevasses into transverse crevasses forming in longitudinal tension, and longitudinal or splaying crevasses forming under longitudinal compression (Glen and Perutz, Reference Glen and Perutz1955; Colgan and others, Reference Colgan2016; Jennings and Hambrey, Reference Jennings and Hambrey2021). While we do identify sectors where crevasses are primarily aligned perpendicular or parallel to the direction of ice flow, they retain a wide distribution of orientations (Fig. 4). For example in the proximal region to the ice front dominated by longitudinal crevasses, crevasses are found oriented in all directions: while crevasses oriented perpendicular to the direction of ice flow is the most abundant, there are secondary populations oriented $\sim \!60^\circ$ and parallel to the direction of ice flow (Fig. 4). Crevasses are oriented almost exclusively parallel to the direction of glacier flow in the zone 5–10 km from the calving front, yet the angle between crevasses and the direction of ice flow is commonly as high as 20–30$^\circ$. Our results are in line with prior studies which have highlighted the complex relation between velocity, strain and measured crevasse orientation, particularly in the case of crevasse fields with multiple closely spaced crevasses (Sassolas and others, Reference Sassolas, Pfeffer and Amadei1996; Harper and others, Reference Harper, Humphrey and Pfeffer1998; Herzfeld and others, Reference Herzfeld, Clarke, Mayer and Greve2004; Colgan and others, Reference Colgan2016). This diversity in measured crevasse orientation and its potential impact on calving behaviour is largely unaccounted for in the current generation of ice-sheet models.

In order for calving to occur, a fracture must propagate through the entire thickness of the glacier and separate one or more fragments of the glacier from the main ice mass. Crevasse orientation is, therefore, a first-order control on calving as transverse crevasses are more easily able to separate icebergs than longitudinal crevasses. In an endmember case with crevasses oriented parallel to ice flow, fracture opening will simply cause the ice front to splay but be unable to detach any icebergs. As our results show, this endmember is not realistic as ice-front conditions and lateral shear margins result in a wider range of crevasse orientations, but some glacier fronts do exhibit a distinctive splaying crevasse pattern (e.g. Glaciar San Quintín, Chile; Svïnafellsjökull, Iceland or Sefstrøms Gletscher, Greenland; Paterson, Reference Paterson1961; Swift and others, Reference Swift2018; Minowa and others, Reference Minowa, Schaefer, Sugiyama, Sakakibara and Skvarca2021). Crevasse orientation can therefore be both a result of a stable glacier front configuration (for instance with longitudinal compression at a pining point) and itself a contributor to stability (with a high angle between crevasses and the ice front inhibiting rapid iceberg calving). Many of the current generation of calving models are calibrated using 1-D or 2-D cross-sectional glacier models (e.g. Benn and others, Reference Benn, Hulton and Mottram2007; Nick and others, Reference Nick, Veen, Vieli and Benn2010; Bassis and Jacobs, Reference Bassis and Jacobs2013; Krug and others, Reference Krug, Weiss, Gagliardini and Durand2014; Lea and others, Reference Lea2014; Bassis and others, Reference Bassis, Berg, Crawford and Benn2021). These models are inherently unable to capture the impact of crevasse orientation on calving rate. Models using a von Mises calving law (e.g. Choi and others, Reference Choi, Morlighem, Wood and Bondzio2018) incorporate both principal stress directions to scale the calving rate, but this remains a necessarily simplified representation of the true crevasse pattern for inclusion in numerical modelling. Crevasse orientation can be evaluated in 3*D discrete element models (Bassis and others, Reference Benn2017; Cook and others, Reference Cook2018; van Dongen and others, Reference van Dongen2020), however, these are computationally intensive and cannot easily be coupled to continuum ice-sheet models. Future studies should aim to parameterize the effect of crevasse orientation on calving rate and iceberg size distributions so that structural glaciology observations can be used to improve forecasts of future ice mass loss. High-resolution, spatially extensive and transient crevasse maps as presented in this study may be used to calibrate such models.

5.4 Future stability of Narsap Sermia

Finally, we consider the implications of our results for the stability and future evolution of Narsap Sermia. The recent retreat of Narsap Sermia has been well documented in previous studies (Motyka and others, Reference Motyka2017; Davison and others, Reference Davison2020), and has persisted through our study period. As of early 2022, the front of Narsap Sermia is 1–2 km up-glacier of its 2016 terminus. Can we gain any insight from our crevasse mapping about whether or not Narsap Sermia is likely to retreat into the overdeepened glacial trough? Firstly, we observe a persistent pattern of longitudinal crevasses ~5–10 km up-glacier of the current ice front. This crevasse pattern is diagnostic of compressional longitudinal stresses (Colgan and others, Reference Colgan2016; Jennings and Hambrey, Reference Jennings and Hambrey2021), for instance at a pinning point, and conducive to glacier stability. Compressional ice flow as ice exits the overdeepened trough might inhibit rapid ice retreat. Secondly, we observe an up-glacier migration of the frontal zone of transverse crevassing, with a gradual increase in the angle between crevasses and ice-flow direction at the transition between the transverse and longitudinal crevassing zones (Fig. 6c). We also observe an increase in ice velocity along the entire central lobe of the glacier, with the largest acceleration occurring close to the ice front. This will be associated with increased longitudinal strain and stress. If longitudinal tension increases sufficiently, it might overcome the present-day compressional flow out of the overdeepened trough, increase ice damage and promote rapid calving. If this does occur, it will likely be preceded by continued up-glacier migration of the zone of transverse crevassing, and overprinting of the current patch of longitudinal crevasses. Real-time monitoring of the crevasse conditions at Narsap Sermia can enable rapid identification of any dynamic change preceding rapid retreat.

6. Conclusions

We use a novel crevasse detection method to map the crevasse pattern of an entire Greenland outlet glacier, Narsap Sermia, across more than 6 years of Sentinel-2 data. Our crevasse detection method, based on filtering optical satellite images using a Gabor filter bank, is able to classify both the location and orientation of individual crevasses. We use this to identify both spatial and temporal patterns in crevassing. The 5 km of Narsap Sermia closest to the calving front is dominated by transverse crevassing, while the central region of the outlet glacier is dominated by longitudinal crevassing, approximately parallel to the direction of glacier flow. Both measured crevasse density and orientation exhibit strong seasonal variability across much of Narsap Sermia, with a seasonal minimum in crevassing in late spring to early summer coincident with a maximum in ice flow speed. Crevassing and velocity also exhibit multiannual changes, with up-glacier propagation of the zone of transverse crevassing coincident with frontal retreat and acceleration. High-resolution, multi-temporal crevasse maps contribute to our understanding of crevasse and calving dynamics, which facilitates forecasting of glacier dynamic change and remains challenging to represent in numerical glacier models.

Supplementary material

The supplementary material for this article can be found at https://doi.org/10.1017/jog.2023.3

Acknowledgements

This research was funded by UKRI Future Leaders Fellowship MR/S017232/1. We acknowledge the editor William Colgan and two anonymous reviewers for their constructive and technical comments, which both improved the clarity of this manuscript and the robustness of our interpretation.

Appendix A. The Gabor crevasse detector

We implement a method to automatically detect and calculate the orientation of crevasses within satellite images using a Gabor filter bank. This method is computationally rapid, extracts individual crevasse orientations and does not require a training dataset. A Gabor filter is a non-symmetrical 2-D Gaussian kernel, modulated in one direction by a sinusoid (Jain and Farrokhnia, Reference Jain and Farrokhnia1990; Kruizinga and Petkov, Reference Kruizinga and Petkov1999; Yang and others, Reference Yang2015). A Gabor filter is therefore modulated by five main parameters: the orientation of the principal axes of the Gaussian θ, the standard deviation of the Gaussian in the rotated x and y directions, the wavenumber of the modulating sine wave λ and the phase of the sinusoid ψ. The complex Gabor filter G θ(x,  y) with a given angle θ is calculated:

(A.1)$$G^{\theta}( x,\; y) = \rm{exp}\left(-{1\over 2}\left[{{\it x_{\theta} }^2\over {\it \sigma_x}^2} + {{\it y_{\theta}}^2\over {\it \sigma_y}^2}\right]\right)\rm{exp}\left(i\left[\psi + {2 \pi \it x_{\theta}\over \lambda}\right]\right)$$

in which x θ and y θ represent the original coordinate system rotated by a given angle θ:

(A.2)$$x_{\theta} = x \; \rm{cos} \, \left(\it \theta \right) + y \; \rm{sin} \,\left(\it \theta \right)$$

and

(A.3)$$y_{\theta} = -x\; \rm{sin}\left(\it \theta \right) + y\; \rm{cos}\left(\it \theta \right).$$

Convolving a given Gabor filter G θ(x,  y) with a given image of a glacier I(x,  y) produces a Gabor response map ${r_G}^{\theta }$:

(A.4)$${r_G}^{\theta} = G^{\theta}( x, \; y) \; \ast \;I( x,\; y) .$$

With a complex Gabor kernel, the response map is also complex with a real and imaginary component. We calculate the final crevasse likelihood map C L and crevasse orientation map C θ by taking the maxima of the Gabor phase at each pixel:

(A.5)$$C_{\rm L},\; C_{\theta} = \rm{max}^ {\it \theta}( \rm{atan2}[ \rm{Re}( {\it r_G}^{\it \theta}) ,\; \rm{Im}( {\it r_G}^{\it \theta}) ] ) $$

with $\rm {Re}( {\it r_G}^{\it \theta })$ and $\rm {Im}( {\it r_G}^{\it \theta })$ being the real and imaginary parts of an individual Gabor response map respectively, and $\rm {max}^{\it \theta}$ representing the maximum across all individual Gabor response maps. The crevasse likelihood is calculated as the maximum value of all individual Gabor response maps, while the crevasse orientation is calculated as the Gabor filter angle θ which produces this maximum value. We then generate a binary crevasse mask C B by thresholding the crevasse likelihood map, with pixels exceeding the empirically calibrated threshold of [1.25 median(C L)] classified as crevasses. Orientations of pixels below the crevasse classification threshold are also discarded. A fully commented implementation of the GCD is available with an example run at https://doi.org/10.5281/zenodo.7319274.

Appendix B. Ice velocity calculation workflow

We calculate displacements from each Sentinel-2 image pair using iteratively reducing multipass template matching following the standard GIV workflow (Van Wyk de Vries and Wickert, Reference Van Wyk de Vries and Wickert2021). We use the standard GIV reference window sizes of 1280, 640 and 320 m (128, 64 and 32 pixels) and a 75% window overlap, for a final velocity-map resolution of 80 m. Displacements are evaluated to sub-pixel precision in the final pass through a Taylor series expansion of correlation values neighbouring the integer extrema. Each pair-wise displacement map is converted into a velocity map by dividing it by the temporal separation between images. We then filter each velocity map by removing the value for pixels that have a signal-to-noise ratio lower than 5 or a peak ratio <1.3, exclude values that differ by more than 50% from their immediate neighbours (four surrounding cells) and 200% from the mean of their larger local area (25 surrounding cells), and interpolate across these now-empty pixels using the values of the remaining (i.e. valid) ice-speed pixels. We do not use a maximum velocity filter so as to capture rapid (>10 km a−1) motion of the glacier front and frontal melange. These thresholds were manually selected based on local tests to exclude the majority of pixels with erroneous velocity estimates based on comparison with neighborring pixels and reference to external datasets (Davison and others, Reference Davison2020; Lei and others, Reference Lei, Gardner and Agram2021). To correct for georeferencing error, we fit a 2-D polynomial surface to the velocities of non-glacierized (stable) areas in the x and y directions for each image pair, and subtract this to the velocities across the entire image.

We calculate a time series of velocities for each pixel, and average all individual velocity maps into a median velocity map and flow direction map covering the entire 6 year period for each of the three image temporal separations (short, medium and long). We compare the velocity time series to the time series of measured crevasse density and orientation, while the median flow direction maps are used to calculate the angle between crevasses and ice flow direction. Nominal strain rates are calculated using the spatial gradient of the NS and EW components of velocity using a central difference scheme for interior data points and a single-sided difference scheme for the edge points. Our offset distance is double the resolution of our velocity grid except for edge points where it is equal to the grid resolution. A tensor rotation is then applied to these gradient maps according to the local flow direction to create the longitudinal strain, transverse strain and shear strain maps (Bindschadler and others, Reference Bindschadler, Vornberger, Blankenship, Scambos and Jacobel1996; Alley and others, Reference Alley2018).

Appendix C. Evaluation of the GCD

We evaluate the GCD by comparing it to two other, previously used crevasse mapping techniques: DEM thresholding and manual delineation (Fig. 9). We obtain a high-resolution (2 mpixel−1) DEM of the front of Narsap Sermia from arcticDEM (Porter and others, Reference Porter2018). Both the DEM and Sentinel-2 scene used to manually delineate crevasses were captured on the same day, 10/09/2016. We high-pass filter the DEM using a 50 × 50 pixel Gaussian kernel, and threshold the resulting elevation anomaly at −0.25 m to delineate crevasses. We manually delineate crevasses using a drawing tablet. We compare the distribution and orientation of crevasses obtained using the three methods. All three methods are correlated, with the binned crevasse orientations from the GCD having a Pearson's r-value of 0.51 and 0.53 with the DEM-derived and manually derived crevasse orientations. All three methods identify a pattern of primarily transverse crevasses in the 5 km nearest to the ice front, with a zone of longitudinal crevassing up-glacier of this. All three methods exhibit a similar histogram of relative crevasse-ice flow directions within the range of 0–25$^\circ$.

Fig. 9. Comparison of measured crevasse orientation maps for the front of Narsap Sermia extracted using the GCD (a), DEM thresholding (b) and manual delineation (c). The inset shows the location and orientation of individual crevasses in one sub-region and a polar histogram of the angle between these crevasses and the direction of ice flow. All three methods identify a region of longitudinal crevassing 5–10 km up-glacier from the calving front.

References

Alley, KE and 5 others (2018) Continent-wide estimates of Antarctic strain rates from Landsat 8-derived velocity grids. Journal of Glaciology 64(244), 321–332. doi:10.1017/jog.2018.23CrossRefGoogle Scholar
Bassis, JN, Berg, B, Crawford, AJ and Benn, DI (2021) Transition to marine ice cliff instability controlled by ice thickness gradients and velocity. Science 372(6548), 1342–1344. doi:10.1126/science.abf6271CrossRefGoogle ScholarPubMed
Bassis, JN and Jacobs, S (2013) Diverse calving patterns linked to glacier geometry. Nature Geoscience 6(10), 833–836. doi:10.1038/ngeo1887CrossRefGoogle Scholar
Benn, DI and 7 others (2017) Melt-under-cutting and buoyancy-driven calving from tidewater glaciers: new insights from discrete element and continuum model simulations. Journal of Glaciology 63(240), 691–702. doi:10.1017/jog.2017.41CrossRefGoogle Scholar
Benn, DI, Hulton, NRJ and Mottram, RH (2007) ‘Calving laws’, ‘sliding laws’ and the stability of tidewater glaciers. Annals of Glaciology 46, 123–130. doi:10.3189/172756407782871161CrossRefGoogle Scholar
Bhardwaj, A, Sam, L, Singh, S and Kumar, R (2016) Automated detection and temporal monitoring of crevasses using remote sensing and their implications for glacier dynamics. Annals of Glaciology 57(71), 81–91. doi:10.3189/2016AoG71A496CrossRefGoogle Scholar
Bindschadler, R, Vornberger, P, Blankenship, D, Scambos, T and Jacobel, R (1996) Surface velocity and mass balance of Ice Streams D and E, West Antarctica. Journal of Glaciology 42(142), 461–475. doi:10.3189/S0022143000003452CrossRefGoogle Scholar
Bondzio, JH, Morlighem, M, Seroussi, H, Wood, MH and Mouginot, J (2018) Control of ocean temperature on Jakobshavn Isbræ's present and future mass loss. Geophysical Research Letters 45(23), 12,912–12,921. doi:10.1029/2018GL079827CrossRefGoogle Scholar
Borstad, CP and 6 others (2012) A damage mechanics assessment of the Larsen B ice shelf prior to collapse: toward a physically-based calving law. Geophysical Research Letters 39(18). doi:10.1029/2012GL053317CrossRefGoogle Scholar
Brown, CS, Meier, MF and Post, A (1982) Calving speed of Alaska tidewater glaciers, with application to Columbia Glacier.CrossRefGoogle Scholar
Choi, Y, Morlighem, M, Wood, M and Bondzio, JH (2018) Comparison of four calving laws to model Greenland outlet glaciers. The Cryosphere 12(12), 3735–3746. doi:10.5194/tc-12-3735-2018CrossRefGoogle Scholar
Christmann, J and 10 others (2021) Elastic deformation plays a non-negligible role in Greenland's outlet glacier flow. Communications Earth & Environment 2(1), 1–12. doi:10.1038/s43247-021-00296-3CrossRefGoogle Scholar
Chudley, TR and 7 others (2021) Controls on water storage and drainage in crevasses on the Greenland ice sheet. Journal of Geophysical Research: Earth Surface 126(9), e2021JF006287. doi:10.1029/2021JF006287CrossRefGoogle Scholar
Colgan, W and 7 others (2011) An increase in crevasse extent, West Greenland: hydrologic implications. Geophysical Research Letters 38(18), 048491. doi:10.1029/2011GL048491CrossRefGoogle Scholar
Colgan, W and 6 others (2016) Glacier crevasses: observations, models, and mass balance implications. Reviews of Geophysics 54(1), 119–161. doi:10.1002/2015RG000504CrossRefGoogle Scholar
Cook, S and 5 others (2018) Modelled fracture and calving on the Totten Ice Shelf. The Cryosphere 12(7), 2401–2411. doi:10.5194/tc-12-2401-2018CrossRefGoogle Scholar
Cook, SJ, Christoffersen, P and Todd, J (2022) A fully-coupled 3D model of a large Greenlandic outlet glacier with evolving subglacial hydrology, frontal plume melting and calving. Journal of Glaciology 68(269), 486–502. doi:10.1017/jog.2021.109CrossRefGoogle Scholar
Crawford, AJ and 5 others (2021) Marine ice-cliff instability modeling shows mixed-mode ice-cliff failure and yields calving rate parameterization. Nature Communications 12(1), 2701. doi:10.1038/s41467-021-23070-7CrossRefGoogle ScholarPubMed
Davison, BJ and 6 others (2020) Subglacial drainage evolution modulates seasonal ice flow variability of three tidewater glaciers in Southwest Greenland. Journal of Geophysical Research: Earth Surface 125(9). e2019JF005492. doi:10.1029/2019JF005492CrossRefGoogle Scholar
Dell, R, Carr, R, Phillips, E and Russell, AJ (2019) Response of glacier flow and structure to proglacial lake development and climate at Fjallsjökull, South-East Iceland. Journal of Glaciology 65(250), 321–336. doi:10.1017/jog.2019.18CrossRefGoogle Scholar
Eder, K, Reidler, C, Mayer, C and Leopold, M (2008) Crevasse detection in Alpine areas using ground penetrating radar as a component for a mountain guide system. The International Archives of the Photogrammetry, Remote Sensing and Spatial Information Sciences 37, 837–841.Google Scholar
Glen, JW and Perutz, MF (1955) The creep of polycrystalline ice. Proceedings of the Royal Society of London, Series A. Mathematical and Physical Sciences 228(1175), 519–538. doi:10.1098/rspa.1955.0066Google Scholar
Goelzer, H and 41 others (2020) The future sea-level contribution of the Greenland ice sheet: a multi-model ensemble study of ISMIP6. The Cryosphere 14(9), 3071–3096. doi:10.5194/tc-14-3071-2020CrossRefGoogle Scholar
Gong, Y and 6 others (2018) Simulating the roles of crevasse routing of surface water and basal friction on the surge evolution of Basin 3, Austfonna Ice Cap. The Cryosphere 12(5), 1563–1577. doi:10.5194/tc-12-1563-2018CrossRefGoogle Scholar
Goodsell, B, Hambrey, MJ, Glasser, NF, Nienow, P and Mair, D (2005) The structural glaciology of a temperate valley glacier: Haut Glacier d'Arolla, Valais, Switzerland. Arctic, Antarctic, and Alpine Research 37(2), 218–232. doi:10.1657/1523-0430(2005)037[0218:TSGOAT]2.0.CO;2CrossRefGoogle Scholar
Harper, JT, Humphrey, NF and Pfeffer, WT (1998) Crevasse patterns and the strain-rate tensor: a high-resolution comparison. Journal of Glaciology 44(146), 68–76. doi:10.3189/S0022143000002367CrossRefGoogle Scholar
Herzfeld, UC, Clarke, GKC, Mayer, H and Greve, R (2004) Derivation of deformation characteristics in fast-moving glaciers. Computers & Geosciences 30(3), 291–302. doi:10.1016/j.cageo.2003.10.012CrossRefGoogle Scholar
Hudleston, PJ (2015) Structures and fabrics in glacial ice: a review. Journal of Structural Geology 81, 1–27. doi:10.1016/j.jsg.2015.09.003CrossRefGoogle Scholar
Izeboud, M and Lhermitte, S (2023) Damage detection on Antarctic ice shelves using the normalised radon transform. Remote Sensing of Environment 284, 113359. doi:10.1016/j.rse.2022.113359CrossRefGoogle Scholar
Jain, AK and Farrokhnia, F (1990) Unsupervised texture segmentation using Gabor filters. In 1990 IEEE International Conference on Systems, Man, and Cybernetics Conference Proceedings, pp. 14–19.CrossRefGoogle Scholar
Jennings, SJA and Hambrey, MJ (2021) Structures and deformation in glaciers and ice sheets. Reviews of Geophysics 59(3), e2021RG000743. doi:10.1029/2021RG000743CrossRefGoogle Scholar
Jennings, SJA, Hambrey, MJ, Moorman, BJ, Holt, TO and Glasser, NF (2022) Upscaling ground-based structural glaciological investigations via satellite remote sensing to larger-scale ice masses: Bylot Island, Canadian Arctic. Earth Surface Processes and Landforms 47(8), 2130–2150. doi:10.1002/esp.5367CrossRefGoogle Scholar
Jones, C, Ryan, J, Holt, T and Hubbard, A (2018) Structural glaciology of Isunguata Sermia, West Greenland. Journal of Maps 14(2), 517–527. doi:10.1080/17445647.2018.1507952CrossRefGoogle Scholar
Kochtitzky, W and Copland, L (2022) Retreat of Northern Hemisphere marine-terminating glaciers, 2000–2020. Geophysical Research Letters 49(3), e2021GL096501. doi:10.1029/2021GL096501CrossRefGoogle Scholar
Krimmel, RM and Meier, MF (1975) Glacier applications of ERTS images. Journal of Glaciology 15(73), 391–402. doi:10.3189/S002214300003450XCrossRefGoogle Scholar
Krug, J, Weiss, J, Gagliardini, O and Durand, G (2014) Combining damage and fracture mechanics to model calving. The Cryosphere 8(6), 2101–2117. doi:10.5194/tc-8-2101-2014CrossRefGoogle Scholar
Kruizinga, P and Petkov, N (1999) Nonlinear operator for oriented texture. IEEE Transactions on Image Processing 8(10), 1395–1407. doi:10.1109/83.791965CrossRefGoogle ScholarPubMed
Lai, CY and 7 others (2020) Vulnerability of Antarctica's ice shelves to meltwater-driven fracture. Nature 584(7822), 574–578. doi:10.1038/s41586-020-2627-8CrossRefGoogle ScholarPubMed
Lea, JM and 8 others (2014) Terminus-driven retreat of a major southwest Greenland tidewater glacier during the early 19th century: insights from glacier reconstructions and numerical modelling. Journal of Glaciology 60(220), 333–344. doi:10.3189/2014JoG13J163CrossRefGoogle Scholar
Lei, Y, Gardner, A and Agram, P (2021) Autonomous repeat image feature tracking (autoRIFT) and its application for tracking ice displacement. Remote Sensing 13(4), 749. doi:10.3390/rs13040749CrossRefGoogle Scholar
Levermann, A and 5 others (2012) Kinematic first-order calving law implies potential for abrupt ice-shelf retreat. The Cryosphere 6(2), 273–286. doi:10.5194/tc-6-273-2012CrossRefGoogle Scholar
Lhermitte, S and 7 others (2020) Damage accelerates ice shelf instability and mass loss in Amundsen Sea Embayment. Proceedings of the National Academy of Sciences 117(40), 24735–24741. doi:10.1073/pnas.1912890117CrossRefGoogle ScholarPubMed
Masson-Delmotte, V and 17 others (2021) Climate Change 2021: The Physical Science Basis. Contribution of Working Group I to the Sixth Assessment Report of the Intergovernmental Panel on Climate Change. Cambridge, UK and New York, NY, USA: Cambridge University Press, 2391 pp.Google Scholar
Millan, R and 6 others (2019) Mapping surface flow velocity of glaciers at regional scale using a multiple sensors approach. Remote Sensing 11(21), 2498. doi:10.3390/rs11212498CrossRefGoogle Scholar
Minowa, M, Schaefer, M, Sugiyama, S, Sakakibara, D and Skvarca, P (2021) Frontal ablation and mass loss of the Patagonian icefields. Earth and Planetary Science Letters 561, 116811. doi:10.1016/j.epsl.2021.116811CrossRefGoogle Scholar
Moffat, C and 6 others (2018) Seasonal evolution of ocean heat supply and freshwater discharge from a rapidly retreating tidewater glacier: Jorge Montt, Patagonia. Journal of Geophysical Research: Oceans 123(6), 4200–4223. doi:10.1002/2017JC013069CrossRefGoogle Scholar
Morlighem, M and 6 others (2016) Modeling of store Gletscher's calving dynamics, West Greenland, in response to ocean thermal forcing. Geophysical Research Letters 43(6), 2659–2666. doi:10.1002/2016GL067695CrossRefGoogle Scholar
Morlighem, M, Rignot, E, Mouginot, J, Seroussi, H and Larour, E (2014) Deeply incised submarine glacial valleys beneath the Greenland ice sheet. Nature Geoscience 7(6), 418–422. doi:10.1038/ngeo2167CrossRefGoogle Scholar
Mottram, RH and Benn, DI (2009) Testing crevasse-depth models: a field study at Breiamerkurjökull, Iceland. Journal of Glaciology 55(192), 746–752. doi:10.3189/002214309789470905CrossRefGoogle Scholar
Motyka, RJ and 11 others (2017) Asynchronous behavior of outlet glaciers feeding Godthåbsfjord (Nuup Kangerlua) and the triggering of Narsap Sermia's retreat in SW Greenland. Journal of Glaciology 63(238), 288–308. doi:10.1017/jog.2016.138CrossRefGoogle Scholar
Nick, FM, Veen, CJVD, Vieli, A and Benn, DI (2010) A physically based calving model applied to marine outlet glaciers and implications for the glacier dynamics. Journal of Glaciology 56(199), 781–794. doi:10.3189/002214310794457344CrossRefGoogle Scholar
Nick, FM, Vieli, A, Howat, IM and Joughin, I (2009) Large-scale changes in Greenland outlet glacier dynamics triggered at the terminus. Nature Geoscience 2(2), 110–114. doi:10.1038/ngeo394CrossRefGoogle Scholar
Nowicki, SMJ and 8 others (2016) Ice Sheet Model Intercomparison Project (ISMIP6) contribution to CMIP6. Geoscientific Model Development 9(12), 4521–4545. doi:10.5194/gmd-9-4521-2016CrossRefGoogle ScholarPubMed
Nye, JF (1952) The mechanics of glacier flow. Journal of Glaciology 2(12), 82–93. doi:10.3189/S0022143000033967CrossRefGoogle Scholar
Nye, JF (1955) Comments on Dr. Loewe's letter and notes on crevasses. Journal of Glaciology 2(17), 512–514. doi:10.3189/S0022143000032652CrossRefGoogle Scholar
Nye, JF and Mott, NF (1953) The flow law of ice from measurements in glacier tunnels, laboratory experiments and the Jungfraufirn borehole experiment. Proceedings of the Royal Society of London, Series A. Mathematical and Physical Sciences 219(1139), 477–489. doi:10.1098/rspa.1953.0161Google Scholar
Nye, JF and Perutz, MF (1957) The distribution of stress and velocity in glaciers and ice-sheets. Proceedings of the Royal Society of London, Series A. Mathematical and Physical Sciences 239(1216), 113–133. doi:10.1098/rspa.1957.0026Google Scholar
Paterson, WSB (1961) Movement of the Sefstrøms Gletscher North-East Greenland. Journal of Glaciology 3(29), 844–849. doi:10.3189/S0022143000027210CrossRefGoogle Scholar
Pearce, DM and 6 others (2018) The glacial geomorphology of upper Godthåbsfjord (Nuup Kangerlua) in southwest Greenland. Journal of Maps 14(2), 45–55. doi:10.1080/17445647.2017.1422447CrossRefGoogle Scholar
Pfeffer, WT and 7 others (1997) Numerical modeling of Late Glacial Laurentide advance of ice across Hudson Strait: insights into terrestrial and marine geology, mass balance, and calving flux. Paleoceanography 12(1), 97–110. doi:10.1029/96PA03065CrossRefGoogle Scholar
Phillips, E and 6 others (2017) Concentrated, ‘pulsed’ axial glacier flow: structural glaciological evidence from Kvíárjökull in SE Iceland. Earth Surface Processes and Landforms 42(13), 1901–1922. doi:10.1002/esp.4145CrossRefGoogle Scholar
Porter, C and 28 others (2018) ArcticDEM (doi: 10.7910/DVN/OHHUKH).CrossRefGoogle Scholar
Pörtner, HO and 9 others (2019) IPCC special report on the ocean and cryosphere in a changing climate. IPCC Intergovernmental Panel on Climate Change: Geneva, Switzerland 1(3).Google Scholar
Pralong, A and Funk, M (2005) Dynamic damage model of crevasse opening and application to glacier calving. Journal of Geophysical Research: Solid Earth 110(B1), 03104. doi:10.1029/2004JB003104CrossRefGoogle Scholar
Pralong, A, Funk, M and Lüthi, MP (2003) A description of crevasse formation using continuum damage mechanics. Annals of Glaciology 37, 77–82. doi:10.3189/172756403781816077CrossRefGoogle Scholar
Pritchard, HD, Arthern, RJ, Vaughan, DG and Edwards, LA (2009) Extensive dynamic thinning on the margins of the Greenland and Antarctic ice sheets. Nature 461(7266), 971–975. doi:10.1038/nature08471CrossRefGoogle ScholarPubMed
Rivera, A, Corripio, J, Bravo, C and Cisternas, S (2012) Glaciar Jorge Montt (Chilean Patagonia) dynamics derived from photos obtained by fixed cameras and satellite image feature tracking. Annals of Glaciology 53(60), 147–155. doi:10.3189/2012AoG60A152CrossRefGoogle Scholar
Sassolas, C, Pfeffer, T and Amadei, B (1996) Stress interaction between multiple crevasses in glacier ice. Cold Regions Science and Technology 24(2), 107–116. doi:10.1016/0165-232X(96)00002-XCrossRefGoogle Scholar
Swift, DA and 7 others (2018) Terminal zone glacial sediment transfer at a temperate overdeepened glacier system. Quaternary Science Reviews 180, 111–131. doi:10.1016/j.quascirev.2017.11.027CrossRefGoogle Scholar
Thompson, SS and 5 others (2020) Comparing satellite and helicopter-based methods for observing crevasses, application in East Antarctica. Cold Regions Science and Technology 178, 103128. doi:10.1016/j.coldregions.2020.103128CrossRefGoogle Scholar
Todd, J and 10 others (2018) A full-Stokes 3-D calving model applied to a large Greenlandic Glacier. Journal of Geophysical Research: Earth Surface 123(3), 410–432. doi:10.1002/2017JF004349CrossRefGoogle Scholar
van der Veen, CJ (1998) Fracture mechanics approach to penetration of surface crevasses on glaciers. Cold Regions Science and Technology 27(1), 31–47. doi:10.1016/S0165-232X(97)00022-0CrossRefGoogle Scholar
van Dongen, ECH and 5 others (2020) Numerical modeling shows increased fracturing due to melt-undercutting prior to major calving at Bowdoin Glacier. Frontiers in Earth Science 8.CrossRefGoogle Scholar
Van Wyk de Vries, M and Wickert, AD (2021) Glacier image velocimetry: an open-source toolbox for easy and rapid calculation of high-resolution glacier velocity fields. The Cryosphere 15(4), 2115–2132. doi:10.5194/tc-15-2115-2021CrossRefGoogle Scholar
Venteris, ER (1999) Rapid tidewater glacier retreat: a comparison between Columbia Glacier, Alaska and Patagonian calving glaciers. Global and Planetary Change 22(1), 131–138. doi:10.1016/S0921-8181(99)00031-4CrossRefGoogle Scholar
Vieli, A, Funk, M and Blatter, H (2001) Flow dynamics of tidewater glaciers: a numerical modelling approach. Journal of Glaciology 47(159), 595–606. doi:10.3189/172756501781831747CrossRefGoogle Scholar
Vieli, A and Nick, FM (2011) Understanding and modelling rapid dynamic changes of tidewater outlet glaciers: issues and implications. Surveys in Geophysics 32(4), 437–458. doi:10.1007/s10712-011-9132-4CrossRefGoogle Scholar
Yang, K and 5 others (2015) River detection in remotely sensed imagery using Gabor filtering and path opening. Remote Sensing 7(7), 8779–8802. doi:10.3390/rs70708779CrossRefGoogle Scholar
Yu, H, Rignot, E, Morlighem, M and Seroussi, H (2017) Iceberg calving of Thwaites Glacier, West Antarctica: full-Stokes modeling combined with linear elastic fracture mechanics. The Cryosphere 11(3), 1283–1296. doi:10.5194/tc-11-1283-2017CrossRefGoogle Scholar
Zhao, J, Liang, S, Li, X, Duan, Y and Liang, L (2022) Detection of surface crevasses over Antarctic ice shelves using SAR imagery and deep learning method. Remote Sensing 14(3), 487. doi:10.3390/rs14030487CrossRefGoogle Scholar
Figure 0

Fig. 1. Diagram describing the main categories of crevasses, and their formation mechanisms.

Figure 1

Fig. 2. Location of Narsap Sermia in Greenland and within Nuup Kangerlua, and view of the glacier from Sentinel-2.

Figure 2

Fig. 3. Diagram of the main steps involved in the automated crevasse mapping method. A time series of satellite imagery is convolved with a Gabor filter bank, creating maximum Gabor phase and maximum response angle maps. The maximum Gabor phase map is then thresholded to extract a crevasse network, with the orientation of each crevasse obtained from the maximum response angle map.

Figure 3

Fig. 4. Measured crevasse orientation map of Narsap Sermia from 17 April 2022, with inset showing the two key crevasse zones: a zone of transverse crevassing near the ice front, and a zone of longitudinal crevassing up-glacier of this. The polar histograms show the angle between the direction of crevassing and the direction of ice flow in each inset.

Figure 4

Fig. 5. Time series of measured crevasse density (b), measured crevasse orientation relative to the direction of ice flow (c) and ice velocity (d) for the 1 km2 down-glacier zone at the front of Narsap Sermia (a). The dark line represents the median monthly velocity. Note that the y-axes are different to Figs 6 and 7 to highlight the seasonal variation in each location.

Figure 5

Fig. 6. Time series of measured crevasse density (b), measured crevasse orientation relative to the direction of ice flow (c) and ice velocity (d) for the 1 km2 transitional zone ~5 km up-glacier from the front of Narsap Sermia (a). The dark line represents the median monthly velocity. Note that the y-axes are different to Figs 5 and 7 to highlight the seasonal variation in each location.

Figure 6

Fig. 7. Time series of measured crevasse density (b), measured crevasse orientation relative to the direction of ice flow (c) and ice velocity (d) for the 1 km2 up-glacier zone ~10 km up-glacier from the front of Narsap Sermia (a). The dark line represents the median monthly velocity. Note that the y-axes are different from Figs 5 and 6 to highlight the seasonal variation in each location.

Figure 7

Fig. 8. Median ice flow speed (a), effective strain rate (b), measured crevasse orientation seasonality (c), crevasse density seasonality (d) and subglacial topography (e). Measured crevasse orientation and density seasonality are calculated as the average of September 2020 to May 2021 minus the average of June 2020 to July 2020. Note that the apparently large seasonal changes on the southern lake-terminating glacier are highly uncertain, and we do not interpret these. Subglacial topography is obtained from BedMachine v4.0 and is referenced to the local mean sea level (geoid).

Figure 8

Fig. 9. Comparison of measured crevasse orientation maps for the front of Narsap Sermia extracted using the GCD (a), DEM thresholding (b) and manual delineation (c). The inset shows the location and orientation of individual crevasses in one sub-region and a polar histogram of the angle between these crevasses and the direction of ice flow. All three methods identify a region of longitudinal crevassing 5–10 km up-glacier from the calving front.

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