1. Introduction
Rapid glacier retreat in the last few decades has led to major changes in glacier dynamics and arguably induced an increase in glacier hazards like glacial lake outburst floods (GLOFs), rapid glacier surges and glacier collapses/avalanches, among others (Huggel and others, Reference Huggel, Kääb, Haeberli, Teysseire and Paul2002; Moore and others, Reference Moore2009; Wang and others, Reference Wang, Xiang, Gao, Lu and Yao2015; Wang and others, Reference Wang, Liu, Liu and He2020; Kääb and others, Reference Kääb2021). In particular, the number and sizes of glacial lakes and related hazards have continued increasing globally at least since the 1990s (Clague and others, Reference Clague, Huggel, Korup and MCguire2012; Carrivick and Quincey, Reference Carrivick and Quincey2014; Haeberli and others, Reference Haeberli2016; Nie and others, Reference Nie2017; Shugar and others, Reference Shugar2020) which is also the case in Norway (Nagy and Andreassen, Reference Nagy and Andreassen2019; Andreassen and others, Reference Andreassen, Nagy, Kjøllmoen and Leigh2022). Glacial lakes are some of the most dynamic and potentially hazardous glacial features that can be prone to sudden and unpredictable drainages (GLOFs) because of dam failures (Emmer and others, Reference Emmer2022a). As opposed to GLOFs from moraine- or landslide-dammed glacial lakes that usually occur only once, ice-dammed lakes often follow cycles of repeated filling and drainage (Iturrizaga, Reference Iturrizaga, Singh, Singh and Haritashya2011) and can drain through different mechanisms (Tweed and Russell, Reference Tweed and Russell1999; Carrivick and others, Reference Carrivick2017).
The current state of knowledge on ice-dammed lake drainage mechanisms suggests that GLOFs are mostly induced by either lifting of the glacier at high pressures or melting of ice walls, resulting in a subglacial drainage (Nye, Reference Nye1976; Clarke, Reference Clarke1982; Björnsson, Reference Björnsson2010a). Other mechanisms include overspill, breaching of ice dams, syphoning and changes in the subglacial cavity drainage systems (Tweed and Russell, Reference Tweed and Russell1999; Carrivick and others, Reference Carrivick2017). Depending on the drainage mode, GLOFs reach their peak discharge within several hours to 2 d, while non-hazardous drainages can last for a period of up to 3 weeks (Björnsson, Reference Björnsson1992, Reference Björnsson2010a, Reference Björnsson2010b). The underlying mechanisms for the initiation of GLOFs have been subjects of numerous studies (Liestøl, Reference Liestøl1956; Nye, Reference Nye1976; Clarke, Reference Clarke1982; Björnsson, Reference Björnsson1992, Reference Björnsson2010a, Reference Björnsson2010b; Walder and Costa, Reference Walder and Costa1996; Huss and others, Reference Huss, Bauder, Werder, Funk and Hock2007; Carrivick and others, Reference Carrivick2017) including their relation to glacier dynamics and climate variability (Tweed and Russell, Reference Tweed and Russell1999) but we are still lacking understanding of external indicators for the timing and magnitudes of drainages (Ng and others, Reference Ng, Liu, Mavlyudov and Wang2007; Ng and Liu, Reference Ng and Liu2009; Kingslake and Ng, Reference Kingslake and Ng2013; Liu and others, Reference Liu, Cheng and Su2014; Yan and others, Reference Yan, Liu, Zhang, Hu and Chen2017). These knowledge gaps inhibit our ability to predict hazardous GLOFs and develop early warning systems to mitigate life loss and damage (Ng and Liu, Reference Ng and Liu2009; Mergili and others, Reference Mergili, Schneider, Worni and Schneider2011; Wang and others, Reference Wang, Zhang, Yao and An2022).
In situ monitoring of glacial lakes is expensive, time consuming and logistically challenging due to their remote locations (Yang and others, Reference Yang2013). In contrast, changes in these environments can be continuously monitored through remote sensing using optical, multispectral or synthetic aperture radar (SAR) satellite imagery (Racoviteanu and others, Reference Racoviteanu, Williams and Barry2008; Chen and others, Reference Chen2021). Compared to the other two types of satellite data, SAR imagery has an advantage that the data quality is not impaired by clouds (Zhang and others, Reference Zhang, Chen, Tian, Liang and Yang2020). Over recent decades, remote sensing of surface water has increasingly utilised automated mapping with band ratio calculations and machine-learning algorithms (Jain and others, Reference Jain, Lohani, Singh, Chaudhary and Thakural2012; Li and Sheng, Reference Li and Sheng2012; Bhardwaj and others, Reference Bhardwaj2015; Cooley and others, Reference Cooley, Smith, Stepan and Mascaro2017; Barbieux and others, Reference Barbieux, Charitsi and Merminod2018; Zhang and others, Reference Zhang, Chen and Tian2018; Qayyum and others, Reference Qayyum, Ghuffar, Ahmad, Yousaf and Shahid2020; Wangchuk and Bolch, Reference Wangchuk and Bolch2020; Chen and others, Reference Chen2021; Nazakat and others, Reference Nazakat2021), although these studies have mostly focused on large glacial lakes (>0.01 km2) (Wangchuk and Bolch, Reference Wangchuk and Bolch2020), which are a minority among GLOF-prone lakes in Norway (Andreassen and others, Reference Andreassen, Nagy, Kjøllmoen and Leigh2022). For Norway, digital glacier and glacial lake inventories have been produced for three time periods – 1988–97, 1999–2006 and 2018–19 – using Landsat imagery for the first two and Sentinel-2 imagery for the most recent dataset (Andreassen and others, Reference Andreassen, Winsvold, Paul and Hausberg2012, Reference Andreassen, Nagy, Kjøllmoen and Leigh2022). The latest inventory documents a total of 455 ice-contact lakes of variable sizes between 0.00042 and 38.5 km2.
Previous glacier-related hazards in Norway, including GLOFs, are documented by Liestøl (Reference Liestøl1956), Jackson and Ragulina (Reference Jackson and Ragulina2014) and the GLOF database of the Norwegian Water Resources and Energy Directorate (NVE). The latter is based on the events registered from the literature, in situ observations and remote sensing (Kjollmoen and others, Reference Kjollmoen, Andreassen, Elvehoy and Storheil2022). While GLOF research is overwhelmingly dominated by physical science, there is a need to complement remote-sensed, model-based and in situ studies with qualitative methods due to the direct relevance of this research for local communities. Indeed, according to Emmer and others (Reference Emmer2022b), over 95% of GLOF-centred publications from 2017 to 2021 were associated with the physical sciences domain, suggesting a research gap between the social and physical sciences. However, qualitative research can provide relevant information to help fill gaps in natural hazard risk management through combining interviews and informal conversations with relevant actors (Ahmed and Kelman, Reference Ahmed and Kelman2018). In addition to qualitative methods, citizen science can complement quantitative data by involving members of the public in the production of scientific knowledge (Strasser and others, Reference Strasser, Baudry, Mahr, Sanchez and Tancoigne2019).
Given the above knowledge gaps, this study has aimed to combine remote sensing with local knowledge and citizen data collection to identify and fill data gaps in the current national GLOF inventories. The main goals of this research are (1) to evaluate whether non-commercial satellite products are fit to consistently track sub-seasonal changes in small ice-dammed glacial lakes in Norway, including de-icing, lake filling and drainage processes; (2) to test the potential of this new workflow to bridge gaps in the temporal resolution of open-access satellite products through accounts of local people in touristic areas where an installation of expensive real-time monitoring systems is currently unjustified and (3) to present a proof-of-concept using an example of an individual ice cap with four drainage-prone ice-dammed glacial lakes in western-central Norway.
2. Study area
Tystigbreen is a glacier complex located at Strynefjellet northeast of the largest ice mass in mainland Norway, Jostedalsbreen (7.21° E/61.55° N) (Fig. 1). It covers an area of 16.4 km2 within an elevation range between 1288 and 1835 m a.s.l. (Andreassen and others, Reference Andreassen, Nagy, Kjøllmoen and Leigh2022). The climate at Tystigbreen is highly dynamic due to its location on top of a mountain that acts as a divide between maritime fjord areas and continental inland regions, coinciding with an area of strong gradient in annual precipitation sums (Andreassen and others, Reference Andreassen, Winsvold, Paul and Hausberg2012). Precipitation sums per hydrological year vary between 1583 and 3879 mm during the reference period of 1991–2022 (Lussana and others, Reference Lussana, Tveito, Dobler and Tunheim2019; Fig. 2). Annual local mean temperatures fluctuate ~−1.6 ± 0.9 °C, with the warmest temperatures for summer months ranging between 6.2 and 12.6 °C and the coldest winter temperatures between −16 and −6.1 °C (Lussana and others, Reference Lussana, Tveito, Dobler and Tunheim2019; Fig. 2). Typically, January and February are the coldest months of the year, while the warmest temperatures are experienced in July or August.
Map of the study area showing (a) the distribution of glaciers and glacial lakes in Norway, (b) map of the study area of Tystigbreen and downstream areas with previously documented GLOF-generating glacial lakes and (c) Worldview-2 satellite image of Tystigbreen (30 July 2021) with the confirmed and newly identified drainage-prone ice-dammed lakes (lakes 1–4 marked as L1–L4) and the location of the Stryn Summer Ski centre testing a citizen-based data collection for this project. Sources: NVE's glacier and glacial lake outlines 2018–19 (Andreassen and others, Reference Andreassen, Nagy, Kjøllmoen and Leigh2022) (a, b) with manual adjustments (c), Kartverket (a–c), Esri (2022) (c).
Multi-decadal evolution of the annual and winter precipitation (a), and annual and monthly mean temperature (b) at Tystigbreen for the period of 1991–2022 derived from the national gridded dataset seNorge (Lussana and others, Reference Lussana, Tveito, Dobler and Tunheim2019). The hydrological year is defined as the period from 1 September to 31 August (NVE, 1993). Here, ‘winter precipitation’ refers to the accumulation season between 1 October and 30 April.
Tystigbreen has six ice-marginal lakes, four of which are prone to frequent drainages (Fig. 1c). Lakes 1 and 2 (Fig. 1c) have average areas of 0.035 and 0.019 km2 and are located at elevations of 1621 and 1616 m a.s.l., respectively (Andreassen and others, Reference Andreassen, Nagy, Kjøllmoen and Leigh2022). Lakes 3 and 4 are not registered in the national glacial lake database but according to our analysis, lake 3 has an area of 0.021 km2 and is located at an altitude of 1478 m a.s.l., while lake 4 has a lake extent of 0.020 km2 and an elevation of 1412 m a.s.l. A country-scale inventory based on satellite images may miss lakes that are empty at the time of image acquisition, or they may not yet have reached their maximum extents. Based on our sub-seasonal analysis, lake 2 has a larger area than lakes 3 and 4 as opposed to the lake extents listed above. Therefore, several images from different dates should be used to map all glacial lakes with their maximum extents (Andreassen and others, Reference Andreassen, Nagy, Kjøllmoen and Leigh2022). Until now, the glacier complex and its glacial lakes have not been monitored by scientific studies, except for the above country-scale inventories. This is at odds with the fact that the glacier complex is easily accessible due to pre-existing infrastructure including roads, ski lifts and the Stryn heliport. So far, no truly damaging impacts have been documented by the downstream communities due to glacial lake drainages from the Tystigbreen lakes. Regardless of this fact, the hazard exposure may change in the future, and investments into studies of this site are well justified, because it is an ideal study area for testing remotely sensed monitoring approaches in combination with in situ monitoring and witness accounts due to the large number of glacial lakes with different drainage behaviours.
3. Data and methods
3.1 Non-commercial optical satellite imagery
Landsat satellites have provided consistent imagery of the Earth surface since 1972 (USGS, 2012), representing a unique uninterrupted archive over five decades. Currently operational Landsat satellites 7–9 record in spectral bands within the visible (VIS), near-infrared (NIR), shortwave infrared (SWIR) and thermal infrared (TIR) spectra. The spatial resolution of the imagery ranges from 15 m for the panchromatic bands to 100 m for the TIR bands, while all the other bands have a resolution of 30 m. This study uses Landsat-8 OLI/TIRS L1T (Operational Lands Imager/Thermal Infrared Sensor Level 1 Tier) products for mapping, complemented by Landsat-7 ETM+ images for visual suitability assessment. Both are corrected for geometric distortion and atmospheric conditions. Landsat-8 OLI L1T images reach a geolocation accuracy of 12 m (Storey and others, Reference Storey, Choate and Lee2014).
Sentinel-2 was launched in 2015 as part of the EU Copernicus programme (ESA, 2015). Sentinel-2 satellites acquire data in 13 spectral bands in VIS, NIR and SWIR spectra. Their spatial resolution ranges from 10 to 20 m for most bands (ESA, 2015). The Sentinel-2 mission is based on a constellation of two satellites positioned at a 180° distance with a repeat cycle of 5 d. Orthorectified and atmospherically corrected L2A (level 2A) as well as Top-Of-Atmosphere corrected L1C (level 1C) scenes were used in this study. The geometric corrections ensure a geolocation accuracy of 12.5 m (Dechoz and others, Reference Dechoz2015).
The PlanetScope mission started in June 2016 and reached daily global coverage with 130 CubeSat satellites between February and July 2017 (PlanetLabs, 2020). PlanetScope imagery has a spatial resolution of 3.7–4.1 m and is recorded in four bands (eight bands since March 2021) in VIS and NIR spectra (Qayyum and others, Reference Qayyum, Ghuffar, Ahmad, Yousaf and Shahid2020) (see Table S1 in the Supplementary material for detailed specifications of the utilised satellite products). This study uses PlanetScope orthoscenes that are geometrically corrected and scaled to surface-reflectance radiance with a reported geolocation accuracy of 10 m. Free access to the PlanetScope satellite data is limited to 5000 km2 per month and is currently only possible through the education and research programme of Planet Labs (PlanetTeam, 2017). Pros and cons of the different satellite missions are listed in Table 1.
Pros and cons of Landsat 7–8, Sentinel-2 and PlanetScope satellite products
3.2 Selection of satellite images
When selecting images for outlining glacial lakes, several criteria must be specified, such as the ablation season, the maximum cloud cover for suitable images and the image quality to minimise cases of misclassification (Racoviteanu and others, Reference Racoviteanu, Paul, Raup, Khalsa and Armstrong2009). Although images acquired around the summer solstice contain fewer cast shadows, Norwegian glaciers during this time are often still covered by snow, and lakes are likely to have ice cover (Nagy and Andreassen, Reference Nagy and Andreassen2019). The latter is an issue for this study since ice-covered lakes are hard to distinguish from ice bodies and snow (Wangchuk and Bolch, Reference Wangchuk and Bolch2020; Chen and others, Reference Chen2021). Here we have defined the ablation season as 1 June to 31 October and have pre-selected all images in which the area around the ice-dammed lakes was not cloud-covered and then assessed whether quality was high enough to visually detect the existence or absence of a waterbody.
3.3 Sub-seasonal glacial lake mapping and GLOF detection
We manually mapped the two largest ice-dammed lakes of Tystigbreen using all pre-selected Sentinel-2 and PlanetScope images (Fig. 3) throughout the ablation seasons between 2016 and 2022 to analyse their filling and drainage behaviours. In addition, we tested a threshold-based indexing method against manual mapping. To automatically extract water from non-water surfaces we used the normalised difference water index (NDWI) (McFeeters, Reference McFeeters1996), which is one of the most widely used indices to classify water in satellite imagery (Hui and others, Reference Hui, Xu, Huang, Yu and Gong2008; Huang and others, Reference Huang, Chen, Zhang and Wu2018). The NDWI is calculated as follows:
Number of suitable images from Tystigbreen during the ablation season (June–October) for the period of 2016–22. All the images from October, except for 2017, are snow covered and thus unfit for a reliable mapping.
Typically, low-threshold values close to 0 are used for the waterbody extraction in ice-free terrain using the NDWI (McFeeters, Reference McFeeters1996; Xu, Reference Xu2006). However, the use of higher threshold values is recommended for the mapping of ice-contact lakes (Nagy and Andreassen, Reference Nagy and Andreassen2019). Here we have adopted a threshold of 0.23 used by Nagy and Andreassen (Reference Nagy and Andreassen2019) when working with the Sentinel-2 imagery. In contrast, visual inspection of the NDWI when using PlanetScope imagery has revealed a need for a different threshold value even though the PlanetScope and Sentinel-2 datasets are radiometrically harmonised. To reconcile this difference, we have calibrated the NDWI method for PlanetScope and found a threshold of 0.1 as most suitable for a binary raster calculation in the target area. To test its skill against manual mapping, we have performed a NDWI classification on all pre-selected PlanetScope and Sentinel-2 images from the ablation season of 2021, since the number of available cloud-free images for this year is some of the largest within the studied period.
3.4 Local knowledge and citizen science
To verify the drainage timing of the glacial lakes, we conducted semi-structured interviews in the community of Hjelledalen, the main impact area of Tystigbreen, during the field campaign in September 2021. During the participant selection process, we utilised a combination of convenience sampling, including criterion and snowball. Our first interviewee was selected through criterion sampling, a purposeful selection method used to identify participants based on pre-defined criteria (Stratford and Bradshaw, Reference Stratford, Bradshaw and Hay2016). Following the initial interview, we located additional interviewees through snowball sampling, a method involving the recommendation of other potential informants by current participants (Stratford and Bradshaw, Reference Stratford, Bradshaw and Hay2016).
As it was important to include different intersections of the population in Hjelledalen, we interviewed a variety of actors who lived or worked in the area. Specifically, we conducted the interviews with participants who varied in occupation, age and gender. To ensure participants were asked questions that generated relevant information, we created an interview guide with open-ended questions that had the purpose to gather qualitative data on participant's knowledge, awareness and perception of glacial lakes and GLOFs. In addition, we carried out informal conversations with local actors, including employees of hotels and staff of camping sites, to complement the data collected during the interviewing process. In total, we conducted six interviews, as well as seven informal conversations (Table 2). The sample size of collected interviews has been adversely impacted by the low number of permanent inhabitants in Hjelledalen. Moreover, some of the potential interview subjects we approached were unable to aid our research since they were lacking knowledge about the glacial lakes of Tystigbreen. Following transcription and review of the qualitative data, we categorised the responses by theme. Relevant information provided by the participants included knowledge on lake drainage, such as time, water levels, sediment transport and velocity.
Local citizens interviewed during field campaigns in September 2021 in Hjelledalen, Stryn, Norway
Through the collaboration with the Stryn Summer Ski centre since spring 2021, we have received access to multi-annual data collected in the field and regular reports and photographic evidence documenting glacial lake levels and drainage events. Using these data, we have tested and refined strategies for the acquisition of photos, starting from a relatively unstructured and occasional sampling and moving towards a more regular documentation from nearly fixed positions at the margin of lake 1 (see Fig. 9).
4. Results
4.1 Mapping of glacial lakes with different satellite products
Our selection of imagery has revealed significant heterogeneities in the availability of high-quality images from different satellite missions across the years (Fig. 3). Prior to July 2017, the PlanetScope mission did not cover the area of Tystigbreen, while starting from 2018, it has consistently offered the largest number of high-quality images during the ablation season due to its close-to-daily coverage of the Earth surface. The only instance when Sentinel-2 and/or Landsat generated more suitable images was in June of 2020–22.
We have estimated the maximum temporal gap between two high-quality PlanetScope images as 36 d (25 June–1 August 2020). This is in contrast to 76 d for Sentinel-2 (26 July–11 October 2018) and 102 d for Landsat (16 July–27 October 2018) (see Table S2 in the Supplementary material). However, regardless of the satellite product, it is challenging to recognise and map the lakes with certainty at the beginning and the end of the ablation season due to early snowfall before mid-October and persistent lake ice and snow cover in June. These limitations impose large uncertainties in our lake reconstructions in the first half of June. Similarly, in all October images but one (9 October 2017), it has been difficult to identify and map those glacial lakes that were not empty at the time of the image acquisition. These difficulties mainly arise from either too extensive snow cover or too low resolution of the images (i.e. Landsat in October 2020). The above issues are further exacerbated by an illumination issue that adversely impacts the quality of the PlanetScope imagery when the surface is snow covered. Thus, its higher image output does not help during the initial and terminal stages of the ablation season.
As demonstrated in two examples in Figure 4, the Landsat-8 imagery is clearly not up to par when it comes to tracking sub-seasonal glacial lake changes or constraining the timing of their drainages. While the two larger lakes (lakes 1 and 2) can be at least identified, the two smaller lakes (lakes 3 and 4; Fig. 4) are unrecognisable in the Landsat-8 images due to their coarse spatial resolution. The temporal resolution of the Landsat-8 imagery is also suboptimal for the studies of the sub-seasonal variations in glacial lakes, especially those that are as small and rapidly changing as the ones at Tystigbreen (Fig. 4). Following these observations, we omitted the Landsat imagery from further analyses.
Detectability of Tystigbreen's glacial lakes in the PlanetScope (left), Sentinel-2 (middle) or Landsat-8 (right) imagery, including the time window constraining the glacial lake drainages for each satellite product. The upper two panels (a) show an example of the drainage event from lake 2 in 2019. The lower two panels (b) depict the drainage of lake 4 in 2021. Projection: WGS1984 UTM Zone 32N.
4.2 Tracking the evolution and drainage of glacial lakes
Using pre-selected PlanetScope and Sentinel-2 images, we manually mapped the extents of lakes 1 and 2 and calculated their respective areas throughout the ablation seasons of 2016–22 (Fig. 5). The small sizes of lakes 3 and 4 and considerable ice cover on all available images where the waterbodies are detectable, hindered their accurate and reliable mapping. To avoid biased results, we therefore excluded them from this analysis. Our results demonstrate that the temporal resolution of the sub-seasonal lake area development can be increased through a combination of the PlanetScope and Sentinel-2 imagery (Figs 5c and f) compared to the mapping based on one satellite product only (Figs 5a and d, b and e). On the one hand, the PlanetScope imagery has made it possible to detect events that would have been missed by the Sentinel-2 image analysis, e.g. lake 1 in 2018 (Fig. 5b, orange). On the other, the identified shortcomings of the PlanetScope images during the early and late stages of the ablation season can be partly compensated through the inclusion of the high-quality Sentinel-2 images (Figs 5a vs b, d vs e).
Development of the areas of lakes 1 and 2 at Tystigbreen throughout the ablation seasons of 2016–22. The two plots on the left (a, d) show the results based on maps derived from the PlanetScope imagery, the two plots in the middle (b, e) show lake areas derived from the Sentinel-2 imagery, and the plots on the right (c, f) show the combined results of PlanetScope- and Sentinel-2-derived lake areas.
The mapping accuracy for the lake areas is adversely impacted by the large variability in the lake surface exposure throughout the years, complicating the comparison between them. For example, the mapped size of lake 1 is abnormally large in 2020 (41 746 m2), which is ~25% larger than average sizes during other years (33 425 ± 1578 m2; Fig. 5). In contrast, the estimated size of lake 2 in 2020 is average but is ~45% larger in 2019 compared to other years (37 614 m2 vs an average of 25 941 ± 2800 m2 during other years). While we cannot obviate the possibility of significant natural fluctuations in the maximum lake filling rate, the above outliers may also mark the mapping uncertainty. Due to geolocation errors of up to 12 m between the PlanetScope and Sentinel-2 images, we could not automatise change detection without pre-processing the imagery. Thus, we have focused our analysis on the changes in absolute lake areas.
Available satellite imagery records only one drainage event for lake 1 that occurred in 2018. In contrast, we have reconstructed complete drainages of lake 2 during all years but 2016 and 2020. The year 2018 is particularly interesting because both lakes appear to have drained within the same time window, which is constrained to a period between 26 July and 13 August (Fig. 5). The lack of data points between these two dates makes it impossible to derive the exact drainage timing and drainage mode (fast vs slow) for each lake, but it is a first indication that simultaneous drainages of the two lakes may be possible in the future.
4.3 Automated vs manual mapping
To quantify the performance of the conventional automated mapping methods such as NDWI on local scales, we compared manually digitised and NDWI-based glacial lake outlines from lakes 1 and 2 throughout the ablation season of 2021. While the manually digitised lake outlines smoothly follow the lake filling process between June and July and capture the drainage of lake 2 in August both with PlanetScope and Sentinel-2 images (Fig. 6), the NDWI-based lake outlines do not correspond to the visual assessment and are thus useless for tracking sub-seasonal lake development (Fig. 7). The NDWI maps fail to reproduce the observed filling and drainage cycle, and our results reveal that the PlanetScope-based mapping is even less consistent with the reality than that based on Sentinel-2 (Figs 6, 7). The NDWI method applied to the PlanetScope imagery introduces noise and misclassified pixels. When applied on Sentinel-2, it tends to exclude floating ice from the lake area (Fig. 7) and classify dark ice (e.g. 12 and 30 July) or shadows as water (e.g. lake 2, 29 August).
Sub-seasonal development of the areas of lakes 1 (a) and 2 (b) using manual vs band-ratio (NDWI) mapping on the PlanetScope (PS) and Sentinel-2 (S2) images. Note the difference in the scales of the y-axis in the plots.
Sub-seasonal development of lakes 1 and 2 based on the manual vs NDWI mapping on the PlanetScope and Sentinel-2 imagery. From top to bottom: manual PlanetScope, NDWI PlanetScope, manual Sentinel-2 and NDWI Sentinel-2. Sources: PlanetScope imagery (rows 1–2) and Sentinel-2 imagery (rows 3–4) from respective dates, NVE glacier outlines are from August 2019 (Andreassen and others, Reference Andreassen, Nagy, Kjøllmoen and Leigh2022).
We used the Sentinel-2 imagery from 30 July to quantify contributions of different sources of misclassification in the NDWI mapping. The lake areas from the manual vs NDWI mapping differ by 5888 m2. Of this difference, 31% originates from the exclusion of the floating ice, and 33.6 and 30.8 are due to misclassification of the dark ice and shadow as water, respectively. The remaining 4.6% of the disagreement between the maps can be presumably attributed to the mapping uncertainty including the impacts of resolution and quality of the images as well as the subjective interpretation of the mapper.
4.4 Results from the interviews and citizen science
During the interviews, five out of six participants admitted that they were aware of potential GLOFs from Tystigbreen but did not think that this phenomenon posed any danger to their community. Four participants remembered changes in the local rivers or glacial lakes during and after the drainage events. For instance, several participants believed that lake 4 drained on 9 June 2021 by observing abrupt changes to both the Tverrelva and Sunndøla rivers during the same period that were not related to a rainfall event. Participant nos. 2, 3 and 5 (Table 2) mentioned changes to the water levels, quality and colour of the river in June 2021. Although the river did not flood, participant nos. 3 and 5 remembered a significant increase of ‘brown’ water in the Tverrelva River that was accompanied by ‘a lot of mud’.
Two participants suggested that lake 1 drained in both 2016 and 2018, but they disagreed on the timing of the 2016 event stating that it either occurred during the summer or the autumn. When comparing the silty water from the drainage in 2021 to the event in 2016, participant no. 3 recalled the water quality of the river as follows:
‘The flood (in 2021) brought in a lot of loose material into the river. However, I find it very interesting that usually when the lakes on the eastern side (Lakes 2–4) drain into Tverrelva, the stream coming out of the glacier is usually very muddy. But the water (in the Videdøla river) coming out under the glacier on the western side of Tystigbreen during this event (Lake 1 in 2016) was not muddy’.
Although participant no. 3 noted that the water draining from the glacier was rather clear, it was also suggested that this was unusual.
In addition to the interviews, participant no. 1 recorded details and provided images of lakes 1 and 2 throughout the seasons of 2021 and 2022. This more frequent monitoring of the sub-seasonal lake changes has made it possible to confirm the drainage of lake 2 in 2021 (Figs 8a and b), constrain the onset of drainage of lake 2 in 2022 (Fig. 8c) and follow the filling of lake 1 in 2022 (Fig. 9). Also, this participant reported hearing cracking noises from lake 1 in October 2021 as a potential sign for a late drainage event of lake 1.
Detected drainage of lake 2 in August 2021 (a and b). The location of the drainage tunnel in (b) is indicated with a red circle (a). (c) The onset of drainage of lake 2 in August 2022. The arrows indicate the maximum water level. Photos: Stryn Summer Ski.
Photographic documentation of the filling of lake 1 in 2022. Photos: Stryn Summer Ski.
4.5 Chronologies of lake drainages and their impacts
Through the analysis of Sentinel-2 and PlanetScope imagery, we were able to detect ten certain and one probable (event 8) drainage events from four ice-dammed lakes of Tystigbreen (Table 3). Two additional events have been reported by local citizens (events 3 and 5), which could not be detected on the satellite imagery. In addition, three events outside the operational periods of Sentinel-2 and PlanetScope are registered in NVE's GLOF database (events 1, 2 and 6) (NVE, 2022). Using interviews with local people and our own analyses presented in this study, we could validate several of the detected drainage events (events 4, 15 and 16) and constrain them to a shorter time window compared to the outcomes of the remote sensing alone. In addition, we could further narrow down the possible time window for lake drainages through a combination of the PlanetScope and Sentinel-2 imagery when compared to the outcomes from a single satellite product (events 11 and 12). Lake 2 has drained every year since 2017 except for 2020 when we could not detect any lake drainages at Tystigbreen. All documented drainages from lake 2 initiated between 20 July and 22 August, corresponding to a mean onset timing on 31 July ± 14 d. Following the drainages, lake 2 was detected as empty (fully drained) between 14 August and 16 September, with a corresponding mean of 28 August ± 11 d. The statistics can also be translated into an average drainage duration of 28 ± 3 d, corresponding to a slow drainage that does not cause floods downstream. Lakes 1, 3 and 4 are assumed to drain at a faster rate as we could identify an exact drainage date (events 2 and 15) and constrain the drainage time window to a maximum of 5 d (events 14 and 16) at least once for each of the lakes.
Drainage events and the timing of drainages of the Tystigbreen lakes detected using the PlanetScope (PS) and Sentinel-2 (S2) imagery, witness accounts (WA) and registered events in the NVE GLOF database
ID stands for event ID. The lake drainages are categorised as certain if they could be detected using two or more sources of information or if they are registered in NVE's database (NVE, 2022).
5. Discussion
5.1 Suitability of optical satellite products for mapping drainage-prone glacial lakes in Norway
Given the focus of this study on sub-seasonal changes in relatively small ice-dammed glacial lakes, we deem both the spatial and temporal resolution of Landsat-8 images insufficient for such tasks (Watson and others, Reference Watson, Quincey, Carrivick and Smith2016). Especially, their lower spatial resolution impedes the detection of smaller glacial lakes such as we find at Tystigbreen (<0.042 km2; Fig. 4), and it is generally problematic for Norway where the majority of glacial lakes are small, with only six of them covering areas larger than 0.2 km2 (Andreassen and others, Reference Andreassen, Nagy, Kjøllmoen and Leigh2022). Also, the low-temporal resolution of Landsat is restrictive towards frequent mapping of drainage-prone glacial lakes of any size, since there are oftentimes only five or fewer cloud-free Landsat-8 images available per season for a given location, with gaps of several months in between (2018, 2019, 2022) (Fig. 3). This is a pity since the Landsat archive goes back to 1972, offering an advantage of mapping surface changes over incomparably longer timescales than Sentinel-2 and PlanetScope. However, the lower spatial resolution of Landsat 1–3 of ~79 m would make mapping small glacier lakes such as those of Tystigbreen even more challenging.
At the other end of the scale, the launch of the PlanetScope mission made it possible to assess small-scale changes (with a spatial resolution of 3–4 m) with a very high-temporal resolution (close to a daily coverage). As shown in Table 3, in many cases it allowed us to constrain the lake drainage timing to the shortest time window (events 4, 8–10, 13 and 15). Yet, it has a lower spectral resolution, with only four bands for most satellites and eight bands for the newest satellites, compared to 11 and 13 bands for Landsat-8 and Sentinel-2, respectively. Furthermore, the PlanetScope imagery is acquired from numerous small CubeSats travelling in different orbits. This causes a weaker spatio-spectral calibration and significant illumination disturbances of the raw images (Houborg and McCabe, Reference Houborg and McCabe2018; Leach and others, Reference Leach, Coops and Obrknezev2019), especially when the surface is snow covered (Fig. 10). If one aims at an automated image analysis, such technical issues would necessitate pre-processing steps such as radiance adjustments, mosaicking and resampling (Latte and Lejeune, Reference Latte and Lejeune2020). In addition, free access to the PlanetScope imagery is currently limited due to requirements of an admission to the education and research programme (PlanetTeam, 2017) and restricted data volume per month. It is therefore difficult to benefit from the full potential of PlanetScope imagery, especially for large-scale mapping exercises.
Comparison of the PlanetScope and Sentinel-2 image quality during the early ablation season. The maps show that the PlanetScope image suffers from illumination disturbances due to the snow cover, while the quality of the Sentinel-2 image is more consistent.
With a 5 d repeat cycle, Sentinel-2 images have only minor shortcomings relative to the PlanetScope imagery but also have a clear advantage such as a stable image quality (Fig. 10). As a result, Sentinel-2 outperforms PlanetScope in the early spring and late autumn when snow cover obstructs the image quality of the latter. Although the PlanetScope imagery was essential for constraining the drainage time periods at the Tystigbreen lakes (Table 3, Fig. 4), it was often assisted by the Sentinel-2 imagery (events 7, 11, 12 and 16). By combining Sentinel-2 and PlanetScope images, we were able to track glacial lake development and detect drainage events with a higher temporal resolution than would be possible with data from only one satellite mission. With the choice of currently available non-commercial imagery, a combination of the Sentinel-2 and PlanetScope products might be therefore the best option for the detection of GLOF events and the associated lake filling and drainage patterns. Especially for the smaller lakes, comparison of the images from both missions would increase the chances of arriving at the right conclusions. However, such combined applications are currently restricted by the limited non-commercial availability of PlanetScope for the public use.
While we show that the combination of the two satellite datasets allows us to track the de-icing, filling and drainage patterns for lakes 1 and 2 throughout individual seasons (Fig. 5), it is unclear why mapped areas of lakes 1 and 2 are considerably larger in one of the analysed seasons (lake 1 in 2020, and lake 2 in 2019). These two instances stand out, since the maximum mapped lake areas are consistent during other years, suggesting that the two outliers may have absorbed the misinterpreted shadowed slopes or lake ice. Due to lack of ground-truthing data and aerial photographs, the time series of lake areas presented here should be considered as rough estimates.
5.2 Validation of automated mapping of sub-seasonal glacial lake changes on local scales
The example of Tystigbreen's glacial lakes demonstrates that automated threshold-based mapping techniques are not effective on local scales, especially for frequent sub-seasonal classification of small ice-dammed lakes (Fig. 7). For larger lakes surrounded by gentler, less shadow-prone slopes, it might be possible to conduct automated sub-seasonal time-series analyses. The uncertainties in the mapping accuracy are higher for smaller lakes, because of a larger significance of single pixels for the total estimated area (Shukla and others, Reference Shukla, Garg and Srivastava2018). Our results using NDWI for glacial lake extraction and tracking have revealed common misclassification of shadowed slopes and blue ice as water and exclusion of lake ice from the lake outlines. As we show on the example of lake 1 on 30 July, 95.4% of the deviation of the Sentinel-2-based NDWI from the manually derived outline could be accounted for the above-mentioned issues. This is a common problem for the NDWI method as diverse surface objects have similar spectral values as opposed to snow and water which have highly distinct values (Huang and others, Reference Huang, Chen, Zhang and Wu2018; Nagy and Andreassen, Reference Nagy and Andreassen2019).
To obtain correct threshold calculations for different surface types, one needs to ensure a consistent image quality with high spectral and radiometric accuracy, which is critical for the successful application of band-ratio mapping (Goswami and others, Reference Goswami2022). This is however where PlanetScope falls short, with large fluctuations in spectral values of lake surfaces and snow cover obstructing the quality of images between different dates and scenes due to illumination issues (see Section 5.1). It is therefore unsurprising that the results of automated mapping on the Sentinel-2 imagery are superior to those on the PlanetScope images (Figs 6, 7). However, even for Sentinel-2, the results of the band-ratio classification do not pass the quality control against manual mapping (Fig. 6). The method remains sensitive to the external conditions that largely determine the robustness of the mapping outcomes. Under optimal illumination conditions with no shadow or lake ice, the NDWI performs relatively well, while the mapping accuracy drastically drops when some of the typical issues discussed above are present. Although similar issues impact manual mapping too, it is easier to identify and correct for the impacts of floating ice, shadowed slopes and ice cover during manual digitisation of lake outlines.
Even though automated mapping may spare manual labour, it is dubious that the required compromises in mapping accuracy are justified by the reduction of workload, when it comes to local scales of individual ice caps and their ice marginal lakes. Specifically, for studies of GLOF-prone ice-dammed lakes in Norway, which are mostly small, frequent manual mapping is not such an unreasonable task and may be less labour-intensive than manual corrections of erroneous glacial lake outlines inferred from automated mapping (Andreassen and others, Reference Andreassen, Nagy, Kjøllmoen and Leigh2022). This assumption is also supported by larger-scale glacial lake inventories conducted in Uttarakhand, India, that demonstrated superiority of manual mapping based on high-resolution images over a semi-automated mapping tested by Bhambri and others (Reference Bhambri, Mehta, Dobhal and Gupta2015).
5.3 Linking diverse sources to fill gaps in the glacial lake drainage database
Through mapping and visual inspection of the Sentinel-2 and PlanetScope satellite imagery during ablation seasons of 2016–22, we were able to detect ten fairly certain drainage events originating from four active ice-dammed lakes at Tystigbreen (see Table 3). Four of these events were validated through fieldwork and supported by informal interviews with local citizens and collaborators (events 4, 11, 15 and 16). Additional evidence from the fieldwork on 15 June 2022 has allowed us to constrain the timing of the drainage event 16 (Table 3) to a time window of 5 d compared to 11 d based on remote sensing alone (Fig. 11).
Documentation of the drainage of lake 4 between 15 June and 20 June 2022 (5 d). (a) The evidence of the filled lake 4 on 15 June 2022, photographed during the fieldwork. Photo: Ursula Enzenhofer. (b) A PlanetScope satellite image from 20 June 2022, where the lake is empty.
The integration of interviews and photographic documentation into our analysis helped validate our results in two important ways. First, interviews with local people provided us with valuable information regarding past GLOFs, in some cases including their precise timing and duration (event 15) and their diverse signatures in the rivers depending on the likely origin of the flood (events 4 and 15). Local knowledge helped us detect a previously unknown GLOF-generating lake (lake 4; Fig. 11), the drainage of which we were able to capture during our fieldwork in 2022. Second, regular witness reports, including photographic documentation of the lake status (Fig. 9), helped us develop, test and refine methods for future lake monitoring.
As a result, we were able to identify two additional drainage events from lake 1 in October 2021 (event 5) and in 2016 (event 3), which could not be detected through optical remote sensing using the data sources in the present study. While not detectable in the satellite images, our collaborators reported significant noise in the vicinity of the lake due to cracking of the lake ice in October 2021 (event 10), which indicates a drainage of lake 1. The reported loud cracking of the lake ice also anticipates that the event was likely associated with a rapid water discharge leading to high water levels in the downstream hydrological system. This is consistent with the residents' assumptions for other drainage events from this lake. This new information about the nature of drainage events from lake 1 has led us to a hypothesis that drainages may have been induced by high pressures leading to a glacier lift (Nye, Reference Nye1976; Clarke, Reference Clarke1982; Björnsson, Reference Björnsson2010a). However, further research and monitoring is necessary to confirm this hypothesis. While community-based reporting of lake drainage events and their signatures is clearly useful for validating the results of remote sensing, there are also risks of misreporting. This has been exemplified by one case in our study (event 3), where participants suggested a different timing for the occurrence of the event. Regardless of the possible inconsistent reporting, we conclude that the fusion of citizen science with quantitative methods is an invaluable source of information that sometimes cannot be captured by optical remote sensing alone.
The national GLOF database includes only three GLOF events from the lakes at Tystigbreen, two of which are dated back to 2010 and 2014 (NVE, 2022). Only one of the ten certain drainage events detected by our sub-seasonal glacial lake analysis within the period of 2016–22 is registered in the national database (event 12) (NVE, 2022). However, most of the detected drainage events (five events where event 8 is uncertain as it was only detected on the PlanetScope imagery) originate from lake 2, which according to our analysis, drains slowly over a period of 1–4 weeks. This slow drainage pattern indicates that drainage of lake 2 is likely induced by melting of ice walls and/or changes in the subglacial cavity drainage system rather than lifting of the glacier (Björnsson, Reference Björnsson1992, Reference Björnsson2010a, Reference Björnsson2010b; Tweed and Russel, Reference Tweed and Russell1999; Carrivick and others, Reference Carrivick2017). Such slow and non-hazardous events are typically defined as lake drainages rather than GLOFs. Nevertheless, the lake drainage behaviour may change with time following further retreat and thinning of the glacier wing that dams lake 2, as has been observed in other cases in Norway such as Demmevatnet (Elvehoy and others, Reference Elvehoy2002) and Koppangsbreen (Jackson and Ragulina, Reference Jackson and Ragulina2014).
Furthermore, we found that the two largest lakes at Tystigbreen have the potential to drain more or less simultaneously as was the case in 2018 (Fig. 5). While this dual event might have been the result of an unprecedentedly hot summer in south-western Norway (Skaland and others, Reference Skaland2019), such extreme summers will likely become more frequent in the future (Pachauri and others, Reference Pachauri2014; Skaland and others, Reference Skaland2019). The identified potential for simultaneous drainage events from several lakes provides a strong motivation for their monitoring through the ablation season that also happens to coincide with the high season for tourism in the area. However, as demonstrated here, this task is not trivial thanks to the limitations of the current open-access satellite products. Currently, the installation of lake-monitoring systems is not a priority because of the non-hazardous nature of the documented lake drainages and the small permanent population of the downstream areas. Hence, the systematic observations by local citizens can serve as sources of validation for remote sensing and information about potential switches between slow and rapid lake drainage styles.
6. Conclusions
Our study combines remote sensing, qualitative methods and citizen science to highlight advantages and limitations of different satellite products and quantify the added value of local knowledge for the monitoring of sub-seasonal ice-dammed lake changes and glacial lake drainage events. Using the case of four ice-dammed lakes of the Tystigbreen glacier, the resolution of the Landsat-8 imagery is deemed insufficient for such analyses. Based on a combination of PlanetScope and Sentinel-2 images, we were able to detect ten glacial lake drainage events and constrain their timing with a precision of 5–32 d. While the high spatial and temporal resolution of PlanetScope is useful for detecting glacial lakes and tracking lake changes on small scales, automatising their mapping with this satellite product is still challenging due to inconsistent image quality. We suggest that further research should focus on fusing the two satellite products to overcome the above issues of PlanetScope and profit from the more consistent image quality and higher spectral resolution of Sentinel-2.
Here we demonstrate that satellite data analyses can capture most of the reported drainage events from the two largest ice-dammed lakes in our study area, albeit with a relatively low-temporal resolution. The latter is mainly due to frequent cloud cover that limits the number of available images with a clear sight of the lakes. These issues may be overcome combining multispectral images with SAR data in the future. For drainage events outside the main ablation season, we have identified further limitations related to extensive lake ice and snow cover in the early and late stages of the season. Also, our preliminary assessment of the added value of the citizen-based lake monitoring and witness accounts confirms that such data can significantly increase the precision of the remote-sensing analyses and in difficult cases, mitigate the aforementioned shortcomings. Our collaboration with the Stryn Summer Ski centre exemplifies the value of citizen science for obtaining direct constraints on the sub-seasonal glacial lake development. Information collected through interviews with local citizens has helped us identify unrecognised GLOF events and verify the occurrence and timing of previously known events. However, we recognise that the precision and quality of the reported information must be improved if it is to be used for systematic monitoring of glacial lakes and GLOFs.
Supplementary material
The supplementary material for this article can be found at https://doi.org/10.1017/jog.2024.13.
Author contributions
J. M. A. selected, downloaded and prepared the satellite images and conducted the remote-sensing analyses and mapping. I. R. supervised the study design. K. K. B. prepared the interview guide. K. K. B. and J. M. A. conducted and analysed the interviews. J. M. A. and I. R. wrote the manuscript draft with contributions from K. K. B., R. L. and L. M. A. All authors read and commented on the manuscript.
Acknowledgements
This study was conducted as part of the GOTHECA project (https://www.gotheca.com/) and Copernicus bretjeneste/NVE Copernicustjenester. We deeply thank Idar Aaboen and the whole team from the Stryn Summer Ski centre. Their help and support during fieldwork as well as contribution to data collection and continuous monitoring of the lake status was indispensable for the realisation of this study. In addition, we want to express our gratitude to all our interview participants for their valuable contributions to this research. Finally, we are very grateful to the scientific editor, Dan Shugar, and two anonymous reviewers for a prompt and positive review process.
Data
The satellite data used in the study were accessed through the following portal sites (last accessed 23 January 2023): https://earthexplorer.usgs.gov/ (Landsat 7–8), https://scihub.copernicus.eu/ (Sentinel-2) and https://developers.planet.com/explorer/ (PlanetScope). Tystigbreen's glacial lake outlines for lakes 1 and 2 for the seasons 2016–22 are available as dataset from Nasjonalt Vitenarkiv (NVA) at: https://doi.org/10.58059/zbz8-bg39.
Open access
