- 1Departamento de Geografía, Facultad de Arquitectura y Urbanismo, Universidad de Chile, Santiago, Chile
- 2Institut für Geographie, Friedrich-Alexander-Universität Erlangen-Nürnberg (FAU), Erlangen, Germany
- 3VRIIC, Innovación y Creación, Vicerrectoría de Investigación, Innovación y Creación, Universidad de Santiago, Santiago, Chile
- 4Department of Physical and Life Sciences, University of Huddersfield, Huddersfield, United Kingdom
- 5CIGA, Centro de Investigación Gaia Antártica, Universidad de Magallanes, Punta Arenas, Chile
- 6Departamento de Geología, Facultad de Ciencias Físicas y Matemáticas, Universidad de Chile, Santiago, Chile
- 7Geoestudios, San José de Maipo, Chile
- 8CECs, Centro de Estudios Científicos, Valdivia, Chile
This article presents satellite-based monitoring of glacial lakes located in the vicinity of the Southern Patagonian Icefield (SPI) between 1986 and 2023, with a focus on year-by-year changes between 2015 and 2023. Glacial lakes in this region are of importance as their growth represents an indirect response to climate change and has implications for local ecosystems, tourism, and recreation. The growth of glacial lakes also has implications regarding the potential generation of Glacial Lake Outburst Floods (GLOFs), and this study therefore enables a better understanding of the evolution of the GLOF hazard associated with the SPI. Using a total of 93 Landsat and Sentinel-2 satellite images, glacial lakes were mapped with the aid of the Normalized Difference Water Index (NDWI) and visual analysis and differentiated into three distinct types (moraine-dammed, bedrock-dammed, and ice-dammed). In addition, the volume of glacial lake water was estimated using an empirical area-volume scaling approach. Our results show that the number, area and volume of glacial lakes around the SPI have increased by 34%, 29% and 31%, respectively, between 1986 and 2023. The most recent inventory (2023) identified 313 lakes with a total area of 639.09
1 Introduction
Glacial lakes worldwide have increased in area and number over recent decades in response to climate-induced glacier retreat and thinning (Iturrizaga, 2014; Shugar et al., 2020). This trend has been observed by localized studies in the Himalayas (Wang et al., 2013; Bajracharya and Mool, 2010), the Andes (Wilson et al., 2017), and the European Alps (Buckel et al., 2018). Glacial lakes develop when meltwater fills over-deepening proglacial terrain and is then impounded by either moraine or rock-bar dams. Glacial lakes can also form behind ice dams, often being located adjacent to glacial tongues. The increased emergence of glacial lakes is of importance for several reasons. Firstly, glacial lakes have been shown to influence glacier mass balance when in contact with the ice (Miles et al., 2018). They can also impact periglacial ecosystems and downstream hydrology, as well as representing a socio-economic asset (Clason et al., 2023). Importantly, glacial lakes can also be the source of Glacial Lake Outburst Floods (GLOFs), which pose a substantial threat to downstream infrastructure and population centers (Jiang et al., 2018; Dussaillant-Jones et al., 2010). To help prepare for and mitigate the impacts of GLOFs, several recent studies have used glacial lakes inventories to perform GLOF hazard assessments such as Iturrizaga (2014); Bajracharya and Mool (2010); Wilson et al. (2018). In addition to this, other studies have used projections of glacier change to predict the location of future glacial lakes (Frey et al., 2010; Viani et al., 2020). Finally, glacial lakes also act as a water reservoir, storing meltwater and reducing the terrestrial contribution of glaciers to sea level rise (Loriaux and Casassa, 2013).
Advances in remote sensing and Geographic Information Systems (GIS) in recent decades have made it easier to assess spatio-temporal changes in glacial lakes in response to climate change. However, the quantification of lake volume, an important parameter for the assessment of water storage and GLOF potential, is more difficult and cannot be derived directly from satellite imagery. In lieu of detailed bathymetry data that is often unavailable for glacial lakes, recent studies have estimated water volume using lake surface changes derived from Digital Elevation Models (DEMs). This technique, however, is only able to calculate relative volume changes between different time periods. To resolve this issue, many studies have instead estimated absolute lake volumes using empirical area-volume relationships (O’Connor et al., 2001; Huggel et al., 2002; Loriaux and Casassa, 2013; Cook and Quincey, 2015). Using a near-global database, Shugar et al. (2020), for example, used a mixed model that applied different area-volume formulas for small and large glacial lakes to monitor lake volume evolution between 1990 and 2018. The threshold between small and large lakes in this instance was obtained by identifying the bias present for small lakes in the classic power area-volume relationship. The study by Shugar et al. (2020) is notable in that it presents a dataset of glacial lake volume observations which extends our understanding of the area and volume relationship, particularly for larger lakes.
The study presented here focuses on the glacial lakes of the Southern Patagonian Icefield (SPI). This study site is significant in that (1) it forms the biggest ice body outside of Antarctica in the Southern Hemisphere (Meier et al., 2018; Casassa et al., 2014), (2) it is surrounding by the largest concentration of glacial lakes in the Chilean and Argentinean Andes (Wilson et al., 2018) and (3) for the coming decades an increase in the melting of the SPI glacier’s is projected (Bravo et al., 2021). The high frequency of glacial lakes in this region is the result of many of the SPI’s outlet glaciers having undergone a prolonged period of thinning and retreat (Meier et al., 2018; Malz et al., 2018; Foresta et al., 2018). Malz et al. (2018), for example, reports a mean specific glacier mass balance of
1.1 Study area
The SPI is characterized by a marked seasonal temperature variation and spatially variable precipitation patterns. South of 49°S, the precipitation is equally distributed throughout the year, with slight maxima in March and April (Sagredo and Lowell, 2012), yet to the north, there is a marked annual cycle. The longitudinal distribution of precipitation is strongly influenced by the presence of the Andes, which, although presenting relatively low elevations in Patagonia, still generates an extreme precipitation gradient with humid western slopes and arid eastern slopes. Annual and interannual changes in precipitation have been shown to strongly impact the surface mass balance of Patagonian glaciers. In terms of the long-term trend, recent studies suggest possible reductions in the amount of snowfall in this region due to climatic warming. Rasmussen et al. (2007), for example, estimate that there has been a 5% reduction in solid precipitation between 1960 and 1999. This agrees with the findings of García-Lee et al. (2024), who determined an annual upward trend of the freezing level throughout Patagonia between 1951 and 2021.
Wilson et al. (2018) presented the first large-scale inventory of glacial lakes in Chile and Argentina covering the Central Andes, Northern Patagonia and Southern Patagonia, reporting an overall increase in glacial lake area of 27% between 1986 and 2016. This work built upon the findings of Loriaux and Casassa (2013), who reported a 64.9% expansion of glacial lakes in the Northern Patagonia Icefield (NPI) between 1945 and 2011. In this study, we present a multi-temporal inventory of glacial lakes in the vicinity of the SPI (Figure 1), characterizing their physical attributes, water volume, and spatial-temporal distribution using Landsat and Sentinel-2 satellite imagery acquired between 1986 and 2023. This research represents an update of the Wilson et al. (2018) glacial lake inventory for the SPI, reporting changes in glacial lakes on an annual basis between 2015 and 2023 and comparing this to the multi-decadal evolution of these features between 1986, 2000 and 2023. To estimate glacial lake volumes, we applied a newly developed empirical area-volume scaling relationship, representing an advancement over the methods used in previous studies such as O’Connor et al. (2001); Loriaux and Casassa (2013); Cook and Quincey (2015); Shugar et al. (2020). Additionally, this study identifies and discusses past GLOF events originating from the SPI, providing valuable insights for future regional hazard management.

Figure 1. Map (a) shows the location of the Northern Patagonia Icefield (NPI) and Southern Patagonian Icefield (SPI). Map (b) shows the location of the glacial lakes surrounding the Southern Patagonian Icefield (SPI) (indicated by orange circles). Dark grey labels identify the main outlet glaciers of the SPI.
2 Data and methods
2.1 Data sources and glacial mapping criteria
In this study, glacial lakes were mapped only if they were located within or immediately adjacent to the 1945 extent of the SPI outlet glaciers. This search area was chosen as it likely contained lakes that had experienced the most significant changes during the observation period (Loriaux and Casassa, 2013). The boundaries of the outlet glaciers in 1945 were derived from a 1:250,000 scale map created and published in 1954 by the Chilean Geographic Military Institute (Instituto Geográfico Militar, IGM). This map was based on the Trimetrogon aerial photographic survey conducted by the U.S. Army Air Force between December 1944 and March 1945. To enhance the accuracy of the analysis, original Trimetrogon aerial photographs were also utilized, as there were some inaccuracies in the maps.
To complete the multi-temporal glacial lake inventory for the SPI, a total of 93 Landsat and Sentinel-2 satellite images were used, with acquisition dates between 1986 and 2023 (Table 1). The satellite imagery used was selected based on image availability and the presence of snow cover, cloud cover and mountain shadowing. All images were obtained from the United States Geological Survey’s (USGS) Earth Explorer interface (https://earthexplorer.usgs.gov/). Named lakes were identified using 1:50,000 maps available from the IGM and reports from the Argentine Geographic Institute.

Table 1. Summary of the Landsat and Sentinel-2 satellite imagery used for the compilation of the multi-temporal glacial lake inventory (1986–2023).
Each glacial lake mapped was characterized by several quantitative and qualitative attributes, including an identification ID code, name (if available), lake type, central coordinates, elevation, and surface area. Following the guidelines of Wilson et al. (2018) and Carrivick and Tweed (2013), glacial lakes were categorized into three sub-types based on the nature of their impounding dams (Figure 2): (1) moraine-dammed lakes (encompassing all subtypes of moraine dams); (2) bedrock-dammed lakes (situated within bedrock over-deepenings); and (3) ice-dammed lakes (impounded by ice). This categorization was done through visual analysis supported by geomorphological observations made by Davies et al. (2020). These observations included detailed maps of the moraines surrounding the SPI, which were used to help identify the composition of the dams.

Figure 2. Examples of glacial lakes classified as: (a) moraine-dammed (49.32°S, 73.00°W); (b) ice-dammed (49.70°S, 73.15°W); and (c) bedrock-dammed (48.27°S, 73.49°W). Images are natural colour composite pan-sharpened Landsat eight images. The yellow outlines represent lake margins from the 2021 inventory.
To characterize glacial lake changes at a sub-annual scale between 2015 and 2023, when a significant change was observed, we included additional images to increase the temporal resolution of the inventory. However, due to the temporal resolution of the satellite data used (e.g., 16 days for Landsat eight and 5–10 days for Sentinel-2 data), cloud cover and other data quality issues, often the temporal resolution achieved was not high enough to properly characterize the observed changes. Lakes Argentino (1,368.5
2.2 Glacial lake delineation
Glacial lakes were mapped in this study using a semi-automated approach, combining the use of the normalized difference water index (NDWI) (McFeeters, 1996) and manual editing. The NDWI is calculated following Equation 1:
where
The Normalized Difference Water Index (NDWI) has been widely used in glacial lake inventories (Huggel et al., 2002; Zhang et al., 2021). The effectiveness of the NDWI for glacial lake mapping can be hindered by image quality issues, including snow, ice, cloud cover, and mountain shadowing. Shadowed areas are common in mid-latitude mountain regions such as Patagonia and exhibit a spectral signature similar to that of glacial lakes with low turbidity, leading to potential misclassification (Gardelle et al., 2011; Loriaux and Casassa, 2013). In this study, shadow areas were discriminated from each other through the use of a slope map derived from the 2000 Shuttle Radar Topography Mission (SRTM) Digital Elevation Model (DEM) at a 90 m spatial resolution. This slope map was visually inspected together with the satellite imagery to correct any potential misinterpretations (Figure 3).

Figure 3. Example of the high variability of the spectral signature of glacial lakes due to the presence of icebergs and shadowing. Natural color composite image acquired on 3 March 2021. The yellow outlines represent lake margins from the 2021 inventory.
Estimating the mapping errors associated with the glacial lake area calculations is challenging without using high-resolution reference data. Several factors influence this estimation, such as the spatial resolution of the imagery (e.g., Landsat = 15–30 m and Sentinel-2 = 10 m), geometric accuracy of the images (e.g., Landsat = 15 m and Sentinel-2 = 10 m), the expertise of the operator performing the classification, and specific image quality issues previously reported (Paul et al., 2013; Wilson et al., 2018).
Following these considerations, we adopted the error estimation approach proposed by Hanshaw and Bookhagen (2014), as adapted by Lesi et al. (2022). This methodology estimates error as a function of the number of edge pixels in a lake polygon, with adjustments to account for duplicated nodes. Key parameters include the total number of nodes in the lake polygon
The equation used to estimate the error is:
where,
In the original formulation, the number of edge pixels corresponds to the fraction
Following Lesi et al. (2022), we use two different expressions to calculate
For polygons without islands, we estimate the number of inner nodes following Equation 3 as:
where
For polygons with islands, we apply Equation 4 as follows:
where
The total number of nodes for each lake delineation was computed using the exterior.coords
function from the GeoPandas package (Jordahl et al., 2020) in Python 3.9.
Finally, the relative uncertainty
where
Individual glacial lakes were assigned unique identification (ID) numbers. To consistently associate the same ID with corresponding lake outlines identified from different years, an equivalent circular area was first calculated for each lake. This area represents the space a circular lake with the same perimeter as the mapped lake would occupy, allowing for the standardization of irregular lake shapes into a comparable metric. Lakes were then matched by comparing their centroids with those of lakes identified in previous time periods. If the centroid of a lake fell within the equivalent circular area of a previously mapped lake, it was then considered to be the same lake. All lakes that did not meet this criterion were assigned ID letters along with their emergence year (year ID), unless they already had a name. If a lake did not fit within the reference circular area, we evaluated whether the areas of both lakes intersected. If an intersection existed, the compared lake was kept as the reference unless it already had a name. In cases where a name was present, the existing name was preserved, and the lake was renamed only if no reference lake was matched.
To assess area changes, we compared the calculated area of each lake across different time periods. If the most recent area measurement fell within the error range of the earlier measurement, we considered the lake’s area unchanged. If the most recent area exceeded the previous measurement and fell outside the error margin, we concluded that the lake had increased in size. Otherwise, we determined that the lake’s area had decreased.
2.3 Volume estimation
To estimate glacial lake volume, we used the empirical area–volume relationship proposed by Shugar et al. (2020) as a starting point. This approach employs a mixed model with different equations for small and large lakes, using a threshold area of 0.5 km2 to divide the two groups. As this method is widely applied at the global scale, it provides a useful benchmark for evaluating its applicability to glacial lakes in the Southern Patagonian Icefield (SPI). The equations used by Shugar et al. (2020) are described in Equations 6–8.
where
Given the high proportion of small lakes
The best model was found by minimizing the misfit using the coefficient of determination
where SST is the total sum of squares around the mean. The SSE is given by Equation 10 as:
and the SST by Equation 11 as:
where
The root mean squared error (RMSE) was calculated by Equation 12 as:
The fitting process was carried out using the robust least absolute residuals (LAR) algorithm in Matlab Center (2021a), and applied to the entire dataset for each polynomial.
2.4 Characterization of GLOFs from ice-dammed lakes
Lakes have a natural water level variation resulting from changes in water input. However, on ice-dammed lakes, these variations are much larger due to changes in the ice dam and GLOFs that can fully drain a lake due to the formation of a subglacial or englacial channel. When a significant decrease in area was observed in an ice-dammed lake, we assumed it was due to a GLOF, and we chose to timestamp the event using the date of the image in which the area reduction was detected. However, it might have happened anytime between the date of that image and the previous one in the inventory. For each GLOF, we used our area-volume empirical relationship to calculate the water volume evacuated. O’Connor et al. (2001) developed an empirical model correlating this evacuated volume with the peak discharge of the GLOF. We used this model to estimate the peak discharge of all drainage events identified. Both evacuated volume and peak discharge must be considered lower bounds, as it is likely that our images captured the lake before it was fully drained or after it had partially refilled. The peak discharge was estimated using Equation 13 as follows:
where
3 Results
3.1 Glacial lake volume estimation
Our database shows that 85% of the inventoried lakes have areas between 0 and 3
Given the area distribution in our inventory and the issues caused by this discontinuity, a new relationship was developed in this study to improve model accuracy, particularly for lakes with areas smaller than 3
where
The second-order polynomial model,
The resulting models are shown in Figure 4, and the fitting parameters in Table 2. Both models show a reasonable fit to the lake volume data, although

Figure 4. Models
Even though both models introduce some bias in estimating smaller lakes, the statistics for the third-order polynomial suggest that
The mixed model developed consists of two components that require an intercept area value of at least 0.57
where
Based on Equations 15, 16, the mixed model that was evaluated was set out as follows:
where
3.1.1 Finding the best volume estimation mixed model
To address the bias in small lakes and improve the accuracy of the third-order polynomial model
The process began by sorting the lake area data in ascending order and selecting consecutive subsets of area-volume pairs. This process was started with lakes that have areas ranging from 0 to 0.57
For each of these fitted subsets, the intersection point between the power model
The optimal transition point was found to be
By analyzing the residuals of the best-fitting model, it was confirmed that
To improve the accuracy of lake volume estimation, particularly for lakes smaller than 3
where
Figure 5 illustrates the comparison between the mixed model and the model by Shugar et al. (2020), which includes 122 glacial lakes with in situ measurements in its dataset. The differences in lake volume estimations are more pronounced in smaller lakes, where the new model corrects overestimation and better captures variations in volume.

Figure 5. Comparison between mixed models
In addition to estimating lake volume using the mixed model
3.2 Spatial and altitudinal distribution of glacial lakes in 2023
In total, 313 glacial lakes were detected in the 2023 inventory (Figure 6; Table 4), covering an area of 639.09

Figure 6. Spatial distribution of the 313 glacial lakes observed in 2023 by type (a) and size (b). The names correspond to the SPI main glaciers. Lakes Argentino, Viedma and O’Higgins/San Martín were excluded from the inventory as mentioned in the data and methods section (subsection 2.1).

Table 4. Main characteristics (number, area, and water volume) of the glacial lakes inventoried between 1986 and 2023.
In terms of their spatial distribution, smaller glacial lakes (
3.3 Evolution of glacial lakes between 1986 and 2023
The assessment of the temporal evolution of glacial lakes, based on a comparison of the 1986, 2000, and 2015–2023 inventories (Table 5), showed that the number of glacial lakes increased from 233 in 1986 to 313 in 2023, reflecting a 34% rise. The total surface area expanded from 496.56 km2; in 1986 to 639.09 km2; in 2023, representing a 29% increase over the same period. In comparison, the total lake volume increased by 31%, from 26.68
Overall, the mapped glacial lakes exhibited various changes, including expansion, coalescence, shrinkage, disappearance, and detachment from their parent glaciers. As expected, bedrock-dammed lakes demonstrated greater stability, as they are typically smaller and situated in geomorphologically stable basins. In contrast, ice-dammed lakes showed high areal variability, while the most significant growth was observed in moraine-dammed lakes (Figure 8).

Figure 8. Behavior of the three types of glacial lakes: (a) moraine-dammed (black column); (2) ice-dammed (grey column); and (3) bedrock-dammed (white column). Glacial lake volume is represented by the orange, green and purple points, respectively.
Throughout the 37-year observation period (Table 5), a total of 352 lakes were mapped (233 lakes in 1986 and a further 199 lakes mapped between 2000 and 2023). Between 2000 and 2023, the newly emerged lakes accounted for a total area and volume of 15.82
The analysis of the evolution of lakes that existed in 1986 shows that, in 2023 44% maintained their area (n = 155), 29% increased in area (n = 102), 15% reduced their area (n = 52) and 12% disappeared (n = 44). All the disappeared lakes were dammed by ice. Overall, moraine-dammed lake tended to increase their area while bedrock-dammed lakes tended to maintain their area (Figure 9).

Figure 9. Evolution of the number of glacial lakes studied between 1986 and 2023: moraine-dammed lake (black), ice-dammed lake (gray) and bedrock-dammed lake (white). This figure excludes the six new lakes identified in 2023, as they have no reference for establishing a trend.
3.3.1 Type and evolution of new glacial lakes
Between 2000 and 2023 (Figure 10; Table 5), a total of 119 new glacial lakes emerged. In general, an increase in new lakes is observed. Most of these newly created lakes fail to consolidate and thus were drained, although they filled up again in 2021.

Figure 10. Number of new glacial lakes per year studied. Color codes represent the year of formation of the glacial lakes.
These newly formed lakes cover a total area of less than 1.3

Figure 11. Size and spatial distribution of new glacial lakes per year of detection. The names correspond to the SPI main glaciers. Color codes refer to those shown in Figure 10.
Regarding the newly formed lakes identified between 2000 and 2023, the following observations were noted (Figure 12): Ice-dammed lakes proved to be the most unstable, with new ice-dammed lakes emerging almost annually from 2016 onwards, but then disappearing in some cases due to rapid drainage events. New lakes associated with ice-dammed lakes tend to disappear rapidly. This instability was evidenced by the GLOF events recorded in 2016 and 2020, when several lakes experienced dramatic reductions in volume. There are also years, such as 2016 and 2022, in which large increases in ice-dammed lake area were observed, highlighting the dynamic nature of this type of glacial lake. In contrast, newly formed moraine-dammed lakes underwent a more gradual and uniform formation process, with lake growth being initiated as glaciers retreat into over-deepened basins and continuing until the parent glacier becomes detached. New moraine-dammed lakes were found to have formed in 2000, 2015, and 2016, and grew consistently up to 2023. Overall, the moraine-dammed lakes that emerged in 2000 have experienced the most significant growth, tripling in area and increasing their volume fivefold during the observation period. Lastly, bedrock-dammed lakes were found to be the most stable in terms of their area. The greater stability of bedrock-dammed lakes arises from the geological stability of their barriers over time. These lakes initially expanded in area by 21% between 2000 and 2015. This growth slowed significantly between 2015 and 2017, before remaining relatively stable between 2017 and 2023, with a slight reduction in area observed by 2023 (Figure 12). No new bedrock-dammed lakes appeared after 2016. The difference in the growth trends of each of the glacial lake types is shown in Figure 12 and is particularly evident between 2015 and 2023.

Figure 12. Evolution of new glacial lakes by types. Lake area and volume are represented by bars and dots, respectively. Color codes refer to those shown in Figure 10.
3.4 Recent dynamics of glacial lakes between 2015 and 2023
Between 2015 and 2023, several large GLOF events were observed in the SPI (Figure 13; Table 6). These events were primarily associated with ice-dammed lakes, which exhibit dynamic changes due to the formation of drainage channels through the ice that impounds them (Figure 14). One of the most significant GLOF events during the observation period occurred at the lake dammed by Bernardo Glacier (48.59°S, 73.80°W) on 30 May 2018, when a total of

Table 6. Summary of the GLOF events observed at the lakes studied between years 2015 and 2023 with the mean dh/dt of their associated glacier as calculated by Malz et al. (2018).

Figure 14. Before (yellow) and after (green) images of ice-dammed lakes with the largest dected changes in area. Lake area during the year of dection is shown in red.
Other important lakes that have produced GLOFs during the observation period are the lakes dammed by Chico, Viedma and Occidental glaciers. At the lake dammed by Chico Glacier (48.98°S, 73.13°W), cycles of lake filling and emptying are observed, where the lake during emptying periods becomes two smaller lakes. The lake dammed by Viedma Glacier (49.54°S, 73.05°W) has also undergone a number of filling and emptying cycles. This lake recorded its smallest area on 7 July 2020 (0.37
It is worth mentioning that, as Figure 14; Table 6 show, all observed drainage events associated with ice-dammed lakes are indistinctly referred to as GLOF events hereafter. However, we have not identified the exact timing of each emptying episode.
4 Discussion
4.1 Methodological biases and limitations
Our methodological approach opened the possibility to produce a large and detailed dataset for studying glacial lakes and their evolution through time at decadal and annual scales. However, some of the processes we have studied, such as GLOFs, have annual periodicity and can exhibit significant changes at a daily scale. Consequently, our estimates of GLOF frequency may be influenced by the temporal availability of imagery. For example, years with more images have a higher likelihood of capturing a GLOF event. Similarly, the timing of image acquisition within a year may introduce bias, as ice-dammed lakes are more or less likely to be in a filled or drained state depending on the month. In the case of our lake volume calculations, for simplicity and due to the scarcity of validation data, we have treated all glacial lakes as equal, even though different processes have formed, which could result in differing area-volume relationships (Cook and Quincey, 2015). Nevertheless, as Shugar et al. (2020), this study neglects such differences and, therefore, the volume estimations reported must be considered first-order approximations.
4.2 Evolution of glacial lakes between 1986 and 2023
Between 1986 and 2023, the number, area, and volume of glacial lakes surrounding the SPI increased by 34%, 29%, and 31%, respectively. By 2023, this study identifies the existence of 313 lakes with a total volume of 34.84
Using geodetic methods, several studies have reported large ice mass losses for the SPI since the 1980s (Rignot et al., 2003; Jacob et al., 2012; Willis et al., 2012; Dussaillant et al., 2019) with Malz et al. (2018) reporting an overall specific mass balance of −0.941
From 1986 to 2023, 119 newly emerged lakes were recorded. Taking 1986 as a reference, we looked into the factors promoting the formation of new glacial lakes and the history of their development in relation to their dam type. Among these, bedrock-dammed lakes are usually smaller and offer relatively less variability with respect to area and volume after the peak achieved in 2017 (Figure 12).
On the other hand, ice-dammed lakes are much more variable. Although year after year, new ice-dammed lakes develop, their number is smaller, and they do not last long as opposed to the moraine and bedrock-dammed lakes (Figure 12). This characteristic reflects the observed variability in ice-dammed lakes driven by the drainage and refilling cycles associated with their ice-dam dynamics.
The non-linear nature of the area–volume relationship used means that a relatively small number of large lakes can contain a disproportionately high proportion of the total lake volume. On the other hand, small lakes are more numerous and, therefore, can have a large water volume. However, we found that small lakes are not numerous enough to compensate for their much smaller individual volumes, and a small number of large lakes monopolizes the water storage reported in our inventory. This was also true for ice-dammed lakes in the periods of 1986–2015 and 2019–2023, when large changes in lake size occurred in the two biggest ice-dammed lakes, dammed by the Pio XI and Bernardo glaciers. This is especially relevant as ice-dammed lakes pose the highest GLOF hazard. This highlights the importance of establishing continuous monitoring of these lakes, especially because of their sustained increase in number and size. New lakes formed between 1986 and 2023 account for around 15.82
4.3 Glacial lake area-volume relationships: Evaluation of the mixed model approach
As discussed in section 4.2, lakes that have a larger surface area tend to have a disproportionately large impact on water storage. This relationship can also be found when using our mixed approach and has been pointed out in previous studies (e.g., Shugar et al., 2020; Loriaux and Casassa, 2013; Huggel et al., 2002; O’Connor et al., 2001; Cook and Quincey, 2015). In Figures 4, 5, we can see how the model calibrated by Shugar et al. (2020) and by us show how both the model calibrated by Shugar et al. (2020) and our own calibration produce increasingly steep curves for larger lakes, highlighting that lake volume grows disproportionately faster than area as lake size increases. This explains why two ice-dammed lakes, dammed by Pío XI and Bernardo glaciers, make the most significant contribution to the volume increases shown for 1986 to 2015 and from 2019 to 2023.
4.4 Ice-dammed lakes and drainage events
The Southern Patagonian Icefield (SPI) experienced significant variability regarding the formation and evolution of new glacial lakes, particularly in the northern section (Figure 11). The retreat of glaciers and climatic variations contributed to the dynamics of these areas, alongside the periodic creation and rapid disappearance of ice-dammed lakes due to drainage events likely associated with GLOF phenomena. This disappearance of ice-dammed lakes can be attributed to drainage that occurred by the thinning of the glacial dam because the increasing water depth can cause ice margin flotation, flexure or fracture, and jökulhlaups (Carrivick and Tweed, 2013). Globally, these lakes represent the most common source of glacier outburst floods (Carrivick and Tweed, 2016). However, some of these disappearances may be due to the fact that the image used for the mapping turned out to be from a moment when the lake was empty, but then could have been filled up again. Because of this uncertainty, we cannot be sure that all accounted drainage events could be associated with GLOF phenomena.
As our results have shown, ice-dammed lake drainage events are particularly common in the northern part of the SPI, where lakes have formed in marginal positions around several of the large outlet glaciers, where the greatest changes in glaciers were observed. In particular, in the glacial systems of Pío XI, Bernardo-Témpanos, O’Higgins-Chico, Viedma and Amalia glaciers (Minowa et al., 2021; Mouginot and Rignot, 2015). Periodic or episodic GLOFs were registered for five lakes, dammed by the Bernardo, Chico, Pío XI, Occidental and Viedma glaciers. These events were marked by changes in lake size and/or the presence of newly exposed lake basins, which, in some cases, were scattered with grounded icebergs (Wilson et al., 2018), like the Occidental and Bernardo glacier events (see Figure 14). In that regard, the analysis of ice-dammed lake change between 2000 and 2023 in this study (Figure 12) highlights the dynamic nature of this type of lake, with observations revealing multiple periods of filling and emptying for individual lakes over relatively short time periods. Several drainage events were observed from five ice-dammed lakes surrounding the SPI, some of which reached peak discharges of up to
In particular, the years 2017 and 2020 recorded the highest frequency of GLOF occurrences, as shown in Figure 13. This peak was associated with a rapid glacier retreat. The frequency of GLOFs was particularly high in areas with widely distributed negative ice elevation changes (Dussaillant et al., 2019). The largest of these drainage events occurred at Lake Greve on 27 June 2020, where an 11% reduction in area in 2 months was observed. We estimate that 3.96
The second most important event is the drainage of the lake dammed by Bernardo Glacier, in which the area reduction wasover 12
Overall, our results highlight the need to monitor ice-dammed lakes in SPI in particular. Globally, ice-dam failure is responsible for the majority of GLOF events (Carrivick and Tweed, 2016). Although the socio-economic vulnerability to drainage events and GLOFs sourced from the SPI is relatively low, due to the low population density of the surrounding region, ice-dammed lakes, in particular, have the potential to threaten tourism in the region. This was demonstrated in October 2023 when the popular ice trekking routes on the Exploradores Glacier (outlet of the Northern Patagonia Icefield) were temporarily closed to tourists. Located in the San Rafael Lagoon National Park in the Aysén region of Chile, the decision to close Exploradores Glacier by the National Forestry Corporation of Chile (CONAF) was partly due to the rapid expansion of an ice-dammed lake located along the eastern flank of the main glacier trunk. As GLOF frequency is likely to increase because of natural and anthropogenic climate change (Emmer et al., 2022), it is crucial to implement monitoring systems on glacial lakes in order to adapt and take a preventive approach. Currently, one such system is being developed by the SAGAZ Project in the Aysén and Magallanes regions (Rada et al., 2024). Further work should also consider GAPHAZ guidelines (Glacier and Permafrost Hazards in Mountains Group), which have already been implemented in the Peruvian Andes (Allen et al., 2022).
5 Conclusion
This study examines the evolution of glacial lake area and volume surrounding the SPI using Landsat and Sentinel-2 satellite imagery acquired in 1986, 2000, and between 2015 and 2023, together with an empirical area-volume mixed model. Overall, an analysis of glacial lakes in the SPI revealed that 44% (n=155) maintained their area, 29% (n=102) increased in size, 15% (n=52) decreased in size, and 12% (n=44) disappeared. These changes come in response to the prolonged period of thinning and retreat observed for many of the SPI’s outlet glaciers. This process of mass loss has resulted in the formation of moraine-dammed, bedrock-dammed and ice-dammed lakes as glacier termini begin to retreat into over-deepened basins. By 2023, we found 313 glacial lakes surrounding the SPI with a total area and volume of 639.09
The results presented in this study have several implications for our understanding of the SPI. Firstly, by using a robust mixed area-volume scaling model, this study provides the most up-to-date assessment of the amount of water stored in the glacial lakes of the SPI. Secondly, the size, distribution, and growth of glacial lakes identified in this study highlight the significant role that these features continue to play in the mass balance of the SPI’s outlet glaciers. Finally, through the observation of numerous drainage events, this study highlights the hazard posed by ice-dammed lake GLOFs in the SPI. These advancements in knowledge will contribute to a better assessment of sea level rise contributions from this region, the modelling of future mass balance changes in the SPI, and the effective management of GLOF risk. Given the dynamic nature of glacial lakes in the SPI, continued monitoring will be necessary in the future. In this regard, this study provides important baseline data and a methodological framework.
Data availability statement
The original contributions presented in the study are included in the article/Supplementary Material, further inquiries can be directed to the corresponding author.
Author contributions
DC: Conceptualization, Data curation, Formal Analysis, Investigation, Resources, Methodology, Visualization, Writing – original draft, Writing – review and editing. JB: Methodology, Investigation, Data curation, Writing – original draft. TL: Investigation, Writing – original draft, Resources. RW: Investigation, Resources, Validation, Writing – original draft. CR: Writing – original draft, Validation, Resources, Data curation, Writing – review and editing. FU: Writing – original draft, Resources, Investigation, Writing – review and editing. CB: Writing – original draft, Resources.
Funding
The author(s) declare that financial support was received for the research and/or publication of this article. JB acknowledge the support of ANID/DAAD through the doctoral scholarships program. TL is funded through Dicyt-Usach 092431CC_Postdoc. FU is funded through Doctoral Scholarship EPEC 2025.
Acknowledgments
We would like to thank Sebastian Pulgar, who started the development of the codes that helped us later on to realize this work. The Sentinel satellite images were provided by the Copernicus mission of the European Space Agency. Landsat satellite images were provided by the United States Geological Survey’s (USGS) Earth Explorer interface (https://earthexplorer.usgs.gov/). The SRTM DEM data was downloaded from the United States Geological Survey. The authors also thank Nicolás Donoso, Nicolás García, Fabiola Gómez and other reviewers for their constructive comments, which helped to improve this manuscript.
Conflict of interest
Author FU was employed by Geoestudios, Las Vertientes.
The remaining authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
Generative AI statement
The author(s) declare that no Generative AI was used in the creation of this manuscript.
Publisher’s note
All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.
Supplementary material
The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/feart.2025.1534451/full#supplementary-material
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Keywords: glacial lakes, Patagonia, lake volume, GLOFs, glacier hazard, remote sensing
Citation: Carrión D, Berkhoff J, Loriaux T, Wilson R, Rada C, Ugalde F and Bravo C (2025) Evolution of glacial lakes in Southern Patagonian Icefield between 1986 and 2023. Front. Earth Sci. 13:1534451. doi: 10.3389/feart.2025.1534451
Received: 25 November 2024; Accepted: 13 June 2025;
Published: 17 July 2025.
Edited by:
Mathias Bavay, WSL Institute for Snow and Avalanche Research SLF, SwitzerlandReviewed by:
Takashi Oguchi, The University of Tokyo, JapanIan Evans, Retired, Durham, United Kingdom
Copyright © 2025 Carrión, Berkhoff, Loriaux, Wilson, Rada, Ugalde and Bravo. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Daniela Carrión, ZGFuaWVsYS5jYXJyaW9uLm9saXZhcmVzQGdtYWlsLmNvbQ==