Professor of Environmental Science at Nichols College in Massachusetts since 1989. Glaciologist directing the North Cascade Glacier Climate Project since 1984. This project monitors the mass balance and behavior of more glaciers than any other in North America
Occidental Glacier in Sentinel images from Dec. 2024 and March 2026 indicating the rapid narrowing of the terminus tongue A, that from the numerous icebergs is actively underway.
Occidental Glacier is an outlet glacier draining west from the Southern Patagonia Icefield. In 2015 the glacier terminus rested on the western shore of a proglacial lake where it bends to the northwest. At Point B a glacier lake was dammed by the ice front. From 2015 to 2021 the northwestern margin of the terminus retreated along the northern shore of the lake. By 2021 the lake at Point B was no longer ice dammed and its water level had declined. The terminus tongue (A) continued to extend to the western shore providing a stable pinning point through 2025.
In 2026 the connection to the western shore has narrowed with the embayment at Point B extending north and east. The terminus tongue (A) on March 22, 2026 is just 850 m wide and actively narrowing, note fresh icebergs. This connection is not stable and will not endure, which will generate significant terminus retreat. This glacier follows neighbors to the north Tempanos and Bernardo Glacier in this process each retreat leading to lake expansion, but also drainage of ice dammed lakes.
Occidental Glacier in Landsat images indicating the retreat of the terminus along the northern shore, the drainage of the embayment at B indicating diminished connection to the western shore of the lake.In 2020 Bernardo, Tempanos and Occidental Glacier had wide terminus tongues terminating in proglacial lakes.By 2026 Bernardo, Tempanos and Occidental Glacier terminus tongues had retreated and narrowed leading to both expansion of proglacial lakes and drainage of a couple ice dammed lakes that the terminus had impounded.
March 21, 2026 was World Day for Glaciers, telling this story is an ongoing four decades long project for us. The North Cascade Glacier Climate Project began in 1984 to identify the response of Washington’s North Cascade glaciers to climate change. The 2026 field season will mark our 43rd year of observations.
I co-direct the project as the science director, with Jill Pelto as the art director. We strive to create a diverse and collaborative portfolio of impactful observations connecting people to science through art and data publication. Our theory of change is that art has the power to inspire people by including the emotional context behind the science research. We seek collaborators who are passionate about contributing to and sharing this work. Here we reflect on some of the stories we have shared in the last 12 months that chronicle the rapidly melting reality of glaciers.
In April, 2025 the “Shaped by Ice” exhibit coordinated by Jill Pelto opened at the Slip Gallery in Seattle. This featured work from nine artists, eight of whom had been in the field with us and was the focus of a Seattle Magazine article.
In May we worked with Protect Our Winters to explore what the loss of glaciers, “Beyond the Ice” means for specific regions.
In June, High Country News focused on the use of art to preserve the legacy of glaciers, given the glaciers themselves are not being preserved.
In March through July we worked with the Global Glacier Casualty List to the tell the story of specific glaciers in the United States that are disappearing, including Ice Worm Glacier in the North Cascades, Darwin Glacier in the Sierra Nevada, Twins Glacier in Wyoming and Burroughs Glacier in Alaska.
In August our field season coincided with a Seattle Time report, on Melting Mountains in the Pacific Northwest means, that we collaborated on.
Joining us in the field on the Lower Curtis Glacier, Mount Shuksan was KING5 NBC-Seattle affiliate, led by Meteorologist Leah Pezzetti who backpacked with us into her first glacier. The logistical preparation for this by KING5 was thorough, and we provided guidance and support to them. The resulting feature was released while we were still in the field.
Upon returning to the trailhead from Lower Curtis Glacier a CBS Sunday Morning News team met us and travelled into the field with us to Sholes Glacier, Mount Baker. The overnight trip into the backcountry was a first for this news team and required extensive collaborative support. The results were shared just two weeks after the filming, and right after our field season.
We worked for a second year with Dan MacComb on a short film for the UN International Year of Glaciers’ Preservation called “Shaped by Ice”. This film published by Protect our Winters has been featured in tfour film festivals during 2025.
In January through February a second “Shaped by Ice” gallery event was held in at the Confluence Gallery in Twisp WA. This was spearheaded by Jill Pelto, Margaret Kingston, and Claire Waichler.
A poor winter snowpack will certainly lead to another year of extensive glacier loss across the Pacific Northwest and we will be there to observe it.
The retreat of the main outlet glaciers of Cook Ice Cap is evident in the Landsat images from 2001 (red arrows) to 2025 (yellow dots). Dumont D’Urville Glacier=-1.5 km, Vallot Glacier=-2.4 km, Naumann Glacier=4.0 km, Ampere Glacier=-3.3 km and Diosaz Glacier=-0.8 km.
Kerguelen Island is at the edge of the furious fifties in the southern Indian Ocean. The island is host to many glaciers, the largest being the Cook Ice Cap at 400 km2. A comparison of aerial images from 1963 and 2001 by Berthier et al (2009) indicated the ice cap lost 21 % of its area in that period. The east side of the Cook Ice Cap outlet glaciers tetreat has led to formation and expansion of a new group of lakes (Pelto, 2016). Here we examine the changes from 2001-2025 along using Landsat and Sentinel imagery.
Ampere Glacier main terminus retreated 800 meters from 2001-2011. Here the terminus has pulled back from the tip of the peninsula on the west side of the terminus and is currently at a narrow point. The eastern terminus has retreated to its junction with the main Ampere Glacier a distance of 1400 m. From 2011 to 2025 the retreat accelerated totalling 3.3 km by 2025. The glacier had two nunataks L and N in 2001, by 2025 L has emerged as a marginal mountain and N is barely surrounded by ice.
Diosaz Glacier retreated 0.8 km from 2001-2025 leading to a small new lake basin developing.
Naumann Glacier retreat has been 4.0 km from 2001-2025 creating an new alpine lake. With the glacier no longer terminating in the lake retreat should slow.
Vallot Glacier has retreated 2.4 km creating a new alpine lake at its southern terminus. The glacier will have just one terminus in the near future and the two lake basins could merge.
Dumon d”Urville Glacier has retreated 1.5 km with the lake it terminates in developing an expanding southern embayment.
The east side of the Cook Ice Cap on Kerguelen Island outlet glaciers retreatn and expanding group of lakes illustrates widespread ice cap thinning (Pelto, 2016). Verfaillie et al (2016) identified that the accelerating glacier wastage on Kerguelen Island was due to reduced net accumulation and resulting rise in the transient snowline since the 1970s, when a significant warming began.
Cook Ice Cap in 2011 Landsat and 2017 Sentinel image. Red arrows indicate 2001 terminus positions and orange dots the 2011 terminus position.
Volcan Peteroa at 35 S straddles the Argentina-Chile Border. Its glaciers-Azufre and Penon have been nearly snow free since mid-January 2026with 5% snowcover on Feb. 16, 2026. These glaciers drain into Rio Colorado and then the Rio Lontue River of Chile.
The summer of 2026 has led to high snow lines and many snow free glaciers in the Central Andes of Argentina and Chile. This follows the pattern observed in 2022, 2023 and 2025 of limited retained snowcover (Pelto, 2025). To be in equilibrium a glacier needs to have 50+% snow cover at the end of the summer. When an alpine glacier such as this loses essentially all snow cover, glacier wide mass balance loss is at least 2 m,. This equates to more than 2 m of thinning on average across the entire glacier.
The Glambie Team (2025) found the southern Andes lost 12.8% of their total mass from 2000-2023. Ayala et al (2025) identified that from 2000-2019 Central Andean glaciers were able to buffer drought conditions in this region. Annual precipitation was 36% below average in this period yet streamflow was essentially maintained. Continued area loss since 2019 is and will lead to ongoing summer runoff declines. This impacts down stream hydropower, aquatic life and agriculture.
From 33 S at Olivares Alfa, to 35 S at Volcan Peteroa False Color Sentinel images illustrate the lack of snow cover in Janurary leading to less than 5% retained snow cover for each of these four glaciated areas.
Cobre Glacier, Argentina flows east from the border. It’s snow cover declined from 20% on Jan. 22, 2026 to 5% on Feb. 18, 2026.The glacier continues to retreat rapidly, the glacier reached the lake at lower right in 2016.The glacier drains into the Rio Grande River.
Humo Glacier and Fiero Glacier, Argentina had 20% snow cover on feb. 18, 2026 declining to 5% snow cover on March 12, 2026. It drains into Lago Atuel and is one of the headwaters of Rio Atuel. Rio Atuel has hydropower development above and within the Rio Atuel Canon including Nihuil dam above the canyon and four more dams within the canyon, including Valle Grande Reservoir.Olivares Alfa Glacier and Paloma Norte Glacier, Chile had less than 10% snow cover on Feb. 16, 2026 declining to less than 5% on March 13, 2026.The glaciers are at the headwaters of the Olivares River, which drains into the Coloardo River. The Alfalfal Hydropower Plant is on the Colorado River.
Glaciar Mayo terminus change from November 2025 to February 2026 illustrated in Sentinel images. The yellow dots indicate the margin, which has retreated on both sides forming a melange (M) and new icebergs (I).
Glaciar Mayo, Argentna in Los Glaciares National Park is an eastern outlet of the Southern Patagonia Ice Cap. The glacier has terminated on the northern shore of a glacial lake for the last ss years. The mass balance from 1975-2011 was identified as slightly positive by Schaefer et al (2015). This enabled the glacier to terminate on the northern shore of a glacial lake, an arm of Lago Argentino from 1984-2020. From 2000-2019 Minowa et al (2021) noted that Glaciar Mayo had transitioned to a negative balance and overall thinning. This thinning is what has led to the terminus beginning to collapse into the lake.
The terminus tongue projecting into the lake had been 2.5 km2, had now declined to 1.4 km2. The terminus along the northern shore had been 2000 m wide and is now 1150 m wide. There is further crevassing/rifting that suggests the glacier tongue is not done thinning in 2026. This continues to be an active year for calving retreat in Patagonia as seen at Upsala and Jorge Montt Glacier, see below.
Glaciar Mayo terminus change from November 2025 to February 2026 illustrated in Landsat images. The yellow dots indicate the margin, which has retreated on both sides forming a melange (M) and new icebergs (I).Jorge Montt Glacier retreat from 2021-2026 with a particularly extensive and packed melanage in 2026, observed in Sentinel images.Upsala Glacier had a burst of calving in Feb. 2026. The comparison to 2021 highlights both the retreat, separation from Bertachhi Glacier and substantial drainage of Lago Guillermo.
Grasshopper Glacier in 2025 Sentinel image with almost no relict ice remaining. To the northwest Wolf Glacier is still an active glacier.
Grasshopper Glacier, Montana is in the Beartooth Range in Custer National Forest. The glacier occupies a north facing cirque at nearly 3300 m on Iceberg Peak (11,000 ft.). The name of the glacier is derived from the millions of grasshoppers that were discovered embedded in the ice in 1898 by Dr. James Kimball. He estimated their were thousand of tons of grasshoppers in the ice. Nearly a century later some of these grasshoppers were extracted from the glacier and using radiocarbon dating scientists the remains of these grasshoppers finding they had been trapped in the 1300s (Sutton et al, 1996). These grasshoppers either were downed by a sudden storm or were carried over the glacier by strong winds aloft, and then cold forced them onto the ice surface. The grasshoppers are an extinct type of Rocky Mountain grasshoppper Melanoplus spretus (Lockwood et al., 1992)
Grasshopper Glacier from the 1966 USGS map, north is at the bottom of this image.
In 1940 the glacier was ~1.6 km. wide and on its northwest side terminated in a 15-m. cliff in a small lake. In 1966, see map below, glacier had an area of 0.42 km2, with a small lake present. The glacier lost 50% of its area and 90% of its volume between the Kimball visit in 1898 and Jane Ferrigno visiting in 1981 (Ferrigno, 1981). In 1981 the upper and lower sections of the glacier are still connecterd, with the bench between them not yet exposed.
Grasshopper Glacier in 1981 illustrating a concave slope, and continuous slope from lake to upper glacier.
By 1994 the area had decline to 0.26 km2. The bench between the upper and lower section of the glacier is emerging and the lake has expanded to 0.08 km2.
Grasshopper Glacier in 1994 Digital Globe image, with red outline indicating 1966 margin. North is at bottom of image. The lake has exapnded substantially.
By 2005 the glacier has separated into a upper portion just below the peak and a narrow section extending to the lake. There is a single crevasse near the ice front. By 2005 this glacier has ceased to exist as an active glacier, there are a few remnant perennial snow and ice patches the largest with an area of 0.05 km2. In the majority of recent summers the glacier has lost all of its snowcover. Glacier survival is dependent on consistent accumulation retained on the glacier each summer, this glacier will not survive.
In 2015 the lower section no longer reaches the lake, and there are no longer any crevasses. The area of the upper section is 0.025 km2. The concave profile, limited area and lack of crevasses indicates this is no longer a glacier.
Grasshopper Glacier in 2005 and 2015 Digital Globe images illustrating the loss of glacier ice reaching the lake. The upper section below Iceberg Peak still has relict ice.
Grasshopper Glacier in 2001 with a few crevasses near the ice front (A.Lussier Image).
The glacier has continued its rapid recession and the further segmentation into small disconnected segments, heralds the end this glacier. We do have a gorgeous new alpine lake in its place. Notice the basin is still largely devoid of plant life, which is red in this false color image. The surface still has the color of newly exposed-deposited sediments. It is interesting that the glacier was named for a type of grasshopper that went extinct in the late 1800s in conjuction with the expansion of farming in the midwest, that disrupted their life cycle. Now the glacier is gone due to the warming climate from our increased production of carbon dioxide.
Novosilski Glacier (N) on the west coast, Risting Glacier (R) in Drygalski fjord, Salomon Glacier (S) on the south shore, Twitcher Glacier (T) in Twitcher Bay and Hindle (Hi) and Ross Glacier (RO) in Royal Bay eachexperienced a detachment (D) from a tributary glacier due to glacier retreat from 2016 to 2016, as noted in these Landsat images.
South Georgia Isalnd is a notoriously cloudy location. A remarkably clear Landsat image from Jan. 21, 2026 provides a good snapshot of glacier change since a similarly clear day on February 19, 2016. Here we examine several glacier near the southern tip of the island that have experienced retreat leading to glacier detachment. Pelto (2017) documented the retreat of 11 of these glaciers during the 1989-2015 period. I worked with NASA Earth to document the retreat of some east coast glaciers evident in Landsat images at that time. BAS map provides context on wildlife populations and glacier retreat.
Novosilski Glacier (N) in 2016 is still connected to Tributary 1. By 2026 tributary 1 is separated from the main glacier due to a 1.3 km retreat.
Novosilski Glacier is a large tidewater outlet glacier on the west (cloudier) coast of South Georgia terminating in Novosilski Bay It shares a divide with the rapidly retreating Ross and Hindle Glacier on the east coast. The glacier retreated 1.3 km from 2020 to 2026 leading to Tributary 1 no longer connecting to the main glacier.
From 2016 to 2026 Ross Glacier retreated 2.5 km and Hindle Glacier 1.6 km. The Hindle retreat led to Tributary 1, 2 and 3 all detaching from one another.
For Ross and Hindle Glacier in 1989 the glaciers joined 2.5 km from the terminus spanning Royal Bay with a 3.2 km wide calving front. By 2001 the glacier front had retreated 800 m, but was still a single joined calving front. By 2009 the glaciers had separated due to an additional retreat of 1.4 km. The Hindle Glacier front was now retreating south up opening a new separate fjord from Ross Glacier. The calving front in 2009 was 1.6 km wide. By 2015 a 1.6 km retreat led to the separation of Hindle from Tributary 4. From 2016 to 2026 a further 1.6 km retreat to the approximate head of the fjord led to separation of Tributary 1, 2 and 3. Ross Glacier retreated 2.5 km from 2016-2026 without separating from any tributary.
A 1 km retreat of Risting Glacier (R) led to Tributary 2 detaching from the Tributary 2 and 3 between 2016 and 2026,
Risting Glacier terminates in Drygalski Fjord on the southeast coast of South Georgia. Risting and Jenkins Glacier were joined until the 1980’s. Cook et al (2010) note the glacier had a relatively uniform retreat rate from 1955-1999 of 40 to 50 meters/year, with retreat increasing after 2000. From 2002-2016 Risting Glacier retreated 1100 m, a rate of ~80 m/year twice the 1955-1999 rate. From2016-2026 the glacier retreated another 800 m, continuing at the same rate. This led to detachment of tributary 1 from the rest of the glacier.
Twitcher Glacier (T) retreated 3.7 km from 2016 to 2026 leading to detachment of Tributary 1.
Twitcher Glacier is the next glacier south of Herz Glacier (H) on the east coast of South Georgia. Until 1989 the glacier ended at the tip of a peninsula that separates it from Herz Glacier., the ensuing retreat has led to the opening of a new fjord. By 2015 the glacier has retreated 2.2 km. An accelerated retreat from 2016-2026 of 3.7 km led to separation from Tributary 1.
The story is the same from glacier to glacier with extensive retreat leading to tributaries detaching from each other. These glaciers still maintain snow cover across a significant area of the glacier and can survive current climate.
Videla Glacier, Chile is an outlet glacier of the Cordillera Darwin Icefield. The glacier has a number (Point 1-6) of terminus lobes where retreat has led to proglacial lake development between 1997 and 2025, as seen in these annotated Landsat images.
Videla Glacier is a land terminating glacier in the northwest portion of the Cordillera Darwin Icefield (CDI) in Tierra del Fuego, Chile. The glacier has terminates in several expanding proglacial lakes each in front of a different tongue of the glacier. The glacier flows northwest from Cerro Ambience towards Fiordo Profundo. Meier et al (2018) identified area change of Patagonia glaciers from 1870-2016 with a ~16% area loss of CDI, with more than half of the loss occurring since 1985. They also noted that CDI glaciers were retreating fastest between 1986 and 2005. Izagirre et al (2025) identified a 124% increase in glacier lake area from retreat between 1945 and 2024. The retreat has been largest on tidewater glaciers such as Marinelli Glacier and Ventisquero Grande Glacier.
In 1997 of Videla Glacier’s six main terminus lobes, five did not exhibit a proglacial lake, only the two northern most lobes (Point 4, 5, and 6) ending in a fringing yet to develop proglacial lake. The terminus lobes at Point 2 and 3 were joined. By 2019 lobes 1 and 4 had developed significant proglacial lakes, while the main terminus at Point 5 and 6 had opened up two halves of the same proglacial lake. The terminus lobes at Point 2 and 3 had separated. A rib (yellow arrow) was developing upglacier of the main terminus indicating thinning and reduced flow. A new lake had developed just downstream of this rib.
In 2025 the terminus at Point 1 had receded 950 m creating a 0.75 km2 proglacial lake. Terminus Lobe 2 and 3 had separated by 400 m. At Point 4 a 0.5 km2 proglacial lake had formed with the 1050 m retreat. The main terminus at Point 5 and 6 extends across the lake basin in a narrow 350 m wide tongue. The lake has grown to 3 km2, with 1.5 km of recession from Point 6 and 1.8 km from Point 5. This narrow tongue may well break off this coming summer.
Videla Glacier, Chile ongoing retreat and proglacial lake growth at terminus lobes (1-6) illustrated by Landsat images from 2019 and 2022.
HPS-12 Glacier in 1985 and 2017 Landsat images. The red arrow indicates 1985 terminus, yellow arrows the 2017 terminus, purple dots the snowline and 1-4 are tributaries. By 2017 all tributaries have detached and the glacier has retreated 13 km.
HPS-12 is an unnamed glacier draining the west side of the Southern Patagonia Ice Cap (SPI). The glacier terminates in a fjord and is adjacent to Upsala Glacier to the east and Pio IX Glacier to the north. This developing fjord is also unnamed but feeds into Estero Falcon. Here we update the 2017 NASA Earth Observatory project I completed in 2017, that identified this as the fastest retreating glacier in Chile in the 1985-2017 period, using Landsat imagery from 1985-2025.
HPS-12 Glacier in 2015 and 2025 Landsat images. The red arrow indicates 1985 terminus, yellow arrows the 2025 terminus, black arrow the 2015 terminus. Former tributary 1 and 2 have declined in width .
In 1985 the HPS-12 terminates 1.5 km from the junction of two fjords that are occupied by HPS-12 and HPS-13. These are separated by a peninsula. The glacier is fed by four tributaries labelled 1-4. The snowline in 1985 is at 900 m. In 2001 the four tributaries still join the main glacier, but the terminus has retreated 3.5 km. In 2015 glacier retreat has led to separation of tributary 1, 2 and 4 from the main glacier, tributary 3 only feeds tributary 2 and not the main glacier. The glacier retreat has continued to 2017, the current terminus is 800 m wide vesus 2800 m wide in 1985 . Total retreat from 1985 to 2017 was 13 km. By 2025 the glacier has retreated 14.75 km and has lost more than 50% of its total length. Tributary 1 and 2 continue to narrow from 2015 to 2025 illustrating that flow from the icefield accumulation zone is being reduced. This suggests less discharge into the terminus reach of HPS-12.
This glacier follows the pattern of retreat we have reported from Bernardo Glacier, O’Higgins Glacier, Tyndall Glacier and Upsala Glacier. The retreat is driven by the SPI have been experienced significant mass loss a. Malz et al (2018) noted a ~1 m/year mass loss from 2000-2016 with HPS-12 and Jorg Montt Glacier losing the most. Minowa et al (2021) found that 35% of all ablation of the Patagonia Icefields stemmed from frontal ablation.
HPS-12 Glacier in 2001 and 2015 Landsat images. The red arrow indicates 1985 terminus, yellow arrows the 2017 terminus, purple dots the snowline and 1-4 are tributaries. By 2015 tributaries 1, 2 and 4 have detached.
Bonnet Glacier in Banff National Park in the 9-5-2025 Sentinel image has lost its snow cover in 2025. This is causing rapid expansion of bedrock amidst the glacier as the glacier thins (yellow arrow).
The summer of 2025 featured extensive melt on Alberta glaciers in many cases removing all snow cover. A glacier that cannot retain snow cover is akin to a company have no income, only expenditures for the year. If this trend persists the glacier will not. This builds on a period of glacier loss in the region from 2011-2020 glacier loss accelerated by ~190% from the 1984-2010 period in this region (Bevington and Menounos, 2022). The 2021-2024 period was noted as a period of unprecedented ice loss in Western Canada (Menounos et al 2025). Haig Glacier has been a summer training ground for cross country skiers. This summer by mid-August snow cover was too limited to permit this use, which had happened in 2023 as well. The result in the images below of rapid melt is fragmentation, bedrock emerging amidst glacier and glacier area decline. Here we examine a series of glaciers within 100 km of Banff, Alberta in Sentinel images from September 2025.
Haig Glacier on 9-2-2025. This glacier in Peter Lougheed Provinicial Park has only a sliver of snowcover at the very top of the glacier.Petain Glacier in Height of the Rockies Provincial Park has a fringe of snow cover left at the top of the glacier in mid-September. The thinning glacier has bedrock emerging amidst the glacier.Icefall Mountain Glacier on 9-5-2025 has lost all snow cover. This glacier in Siffleur Wilderness Area features expanded bedrock areas amidst the glacier (yellow arrows).Trifid Glacier in Banff National Park lost its snowcover and is continuing to fragment in this false color Sentinel image.Drummond Glacier in Banff National Park in early September 2025 has lost 96% of its snow cover this is leading to fragmentation of the glacier.
Willingdon Glacier in Siffleur Wilderness Area lost all but a sliver of snow cover in 2025. The rapid thinning bare glacier ice is leading to fragmentation at yellow arrow.
Rikeva Glacier retreat in Landsat images from 2020 and 2025. Illustrates new island at Point A and retreat of land terminus at Point B and from headland at Point C.
Rikeva (Rykacheva) Glacier flows from the Northern Novaya Zemlya Ice Cap to the west coast and the Barents Sea. The glacier has been retreating rapidly like all tidewater glaciers in northern Novaya Zemlya (Pelto, 2016) (Carr et al 2014) identified an average retreat rate of 52 m/year for tidewater glaciers on Novaya Zemlya from 1992 to 2010. Maraldo and Choi (2025) identified frontal retreat rate of Novaya Zemlya glaciers from 1931-2021 and found an increased each decade since the early 1970s, reaching a peak retreat rate of 65 m/year between 2011 and 2021. We have observed the impact at Vilkitskogo Glacier and Krayniy Glacier,
In 2000 Rikeva Glacier extended beyond the island that would emerge at Point A. The landbased terminus lobe extended just beyond Point B. By 2013 the glacier had retreated adjacent to the island, with the island acting as a stabilizing point for the terminus. The terminus lobe had retreated just south and east of Point B.
Rikeva Glacier in Landsat images from 2000 and 2013 illustrating retreat to island at Point A and retreat of land terminus at Point B.
In 2018 Rikeva Glacier terminus rested on an island at Point A that acted as a buttress for the glacier terminus. By 2025 the glacier had retreated from the island with 4.5 km2 of glacier retreat since 2018 and 8 km2 of retreat since 2000.
Rikeva Glacier in Sentinel images from 2018 and 2025 illustrates retreat from Island at Point A.
Macbeth Icefield, BC in false color Sentinel image from 9-25-2025. Bare of snow cover reveals annual layers within firn, darkened by dust and forest fire partical deposition.Small glaciers A,B,C and E have vanished.
Macbeth Icefield is the Purcell Mountains of southwestern British Columbia. The several icefield outlet glaciers drain into Duncan Lake the Duncan River and then Kootenay Lake. From 2011-2020 glacier loss accelerated by more tha 250% from the 1984-2010 period in this region (Bevington and Menounos, 2022). The 2021-2024 period was noted as a period of unprecedented ice loss in Western Canada (Menounos et al 2025). The summer of 2025 was even worse. Access to the Macbeth Icefield Recreation Area is currently closed due to extensive forest fire impact to the long hiking trail that accesses the icefield (images below illustrate the burn scars).
I have had the opportunity to review satellite images of this area from 1984-2025. In 2025, for the first time the icefield lost all snow cover exposing many annual layers of firn. The firn is snow that endured at least one summer, and is not yet converted to glacier ice. This firn is signficantly darkened by particles of dust and forest fire derived material. This further enhances melt once exposed.
In 2023 and 2024 significant firn areas were exposed as well, in the sequence of images below. . The repeated years of limited snow cover has led to mass balance loss and a 25-30% reduction in icefield area since 1987. From 1987-2025 several small adjacent glaciers have been lost A,B, C and E. t Point D the glacier has fragmented. At Point F the glacier ended in the lake in 1987 and now the glacier has retreated 700 m from the lake.
Macbeth Icefield in 1987 and 2025 Landsat images indicating recession of icefield margin, loss of snowcover and vanished small glaciers A,B,C and E.A 2024 forest fire burned extensive areas in the Birnam Creek valley that drains the southern end of the icefield. The 2023 image illustrated the consistent red of forest, with the brown areas at the yellow arrows indicating burn scars.Macbeth Icefield in Sentinel image from 9-1-2023. Extensive firn area is exposed, while 30% of the icefield has retained snow cover.Macbeth Icefield in Sentinel image from 9-5-2024. Extensive firn area is exposed, while 20% of the icefield has retained snow cover.Macbeth Icefield in Sentinel image from 9-25-2025. The lack of snow cover is evident.
From a Glaciers Perspective 