Belopolskijbreen Retreat Generates Terminus Split, Svalbard

On April 20, 2016May 2, 2024 By mspeltoIn glacier climate change, Glacier Observations, svalbard glacier retreat

Belopolskijbreen comparison in 1990 and 2014 Landsat images. Red arrow is the 1990 terminus location, yellow the 2014 extent of the a bedrock ridge separating the two lobes of the glacier, and purple arrow an area of thinning at the head of the glacier.

Most of the attention on Svalbard glaciers goes to the larger tidewater glaciers, which collectively having been losing volume rapidly. Belopolskijbreen in Sorkappland near the southern tip of Svalbard a land based glacier that we examine here using Landsat images from 1990 to 2014. The glacier is adjacent to Olsokbreen a rapidly retreating tidewater glacier. In 1990 and in the TopoSvalbard maps indicate the glacier terminating in proglacial lakes A and B. The snowline is restricted to the very top of the glacier. With limited retained snowpack anywhere, the glacier will thin and retreat significantly. In the middle of the glacier near the red arrow is a bedrock ridge that 700 m into the glacier. By 2014 the bedrock ridge has extended to the yellow arrow, an additional 700 m. The glacier has retreated 500 m from Lake A and 650 m from Lake B. The retreat of approximately 500 m across a 4 km wide glacier front plus the expansion of bedrock in the middle, represents more than 2 square kilometers of area lost. This retreat will continues as the snowline has been limited to the very top of the glacier in 2013, 2014 and 2015. The 2013 Landsat image below indicates the snowline with purple dots. The snowline is above 375 m with the top of the glacier at just over 400 m. The glacier has 10% snowcover retained at a maximum, the minimum needed for equilibrium is 50%.

Nuth et al (2013) determined that the glacier area over the entire archipelago has decreased by an average of 80 km²per year over the past 30 years, a 7% reduction. In the most recent period 1990-2007, terminus retreat was larger than in an earlier period from 1930-1990, while area shrinkage was smaller. Svalbard is host to 163 tidewater glaciers with a collective calving front of 860 km (Błaszczyk et al, 2009). Blaszczyk et al. (2013) reported the total area of the glacier cover lost in Hornsund Fjord area from 1899–2010 was approximately 172 square kilometers, which is just north of Sorkappland.

TopoSvalbard map of Belopolskijbreen, terminating at Lake A and B. Red arrow marks ridge separating glacier terminus into two lobes.

2013 Landsat images. Note the snowpack limited to the very top of the glacier, purple dots

Goddess of Light (Kolahoi) Glacier Showing Mortality, Kashmir Retreat 1993-2015

On April 14, 2016May 2, 2024 By mspeltoIn glacier climate change, Glacier Observations, Himalaya glacier retreat4 Comments

Kolahoi Glacier comparison in Landsat images from 1993 to 2014. Kolahoi Glacier is the northern glacier, East Kolahoi Glacier the other noted glacier. Red arrows indicate 1993 terminus locations, and yellow arrows the 2014 terminus locations.

The Kolahoi Glacier in Kashmir is known as the—”goddess of light”—Gwash Brani (NatGeo, 2010). The glacier descends the north side of the mountain with two tongues of the glacier merging above the terminus in 1993. The glacier drains into the Liddar River and then the Jhelum River system. The Jhelum River has several large operating hydropower stations and several more under construction including the Karot Hydropower Project a 720 MW run of river project. Jeelani et al (2012) observed that the Liddar Watershed derives 60% of its runoff from snowmelt and just 2% from glacier ice melt. They further report that the Liddar watershed has 17 glaciers covering an area of 40 km² in 2008. The climatic warming in the region has led to mass wasting of Kolshoi Glacier and retreat. From 1970 to 1990 there was a cooling trend of about −0.02°C per year followed by the time period from 1991 to 2010 with the highest increasing trend of 0.07°C per year (Jeelani et al 2012) . Tayal (2011) observed the detachment of the two glacier branches and a loss of 2-3.5 m of ice thickness due to ablation in the lower reach of the glacier.

Hydropower Projects in Jhelum Basin.

From 1993 to 2001 there is limited retreat of Kolahoi Glacier and East Kolahoi Glacier, though both glacier fronts become narrower. By 2006 Kolahoi Glacier has retreated to near the base of a steeper slope. The glacier remains heavily crevassed in the region above the icefall within 1 km of the terminus, Point A. By 2014 the glacier has retreated to the top of the steeper slope between two bedrock knobs at 3650 m, total retreat from 1993 to 2014 is 700 m. Crevassing above the slope, at Point A, that used to be an icefall has become limited since 2006 and before. The reduction in velocity indicates retreat will continue. The western tributary of the Kolahoi has developed a separate termini from the main glacier after 2001, single vertical red arrow.. The East Kolahoi Glacier has retreated 300 m. The lower 300 m of Kolahoi Glacier is thin and relatively uncrevassed. This indicates the retreat will continue. This region has its highest precipitation from January through April and highest runoff in June and July. Hence, the glacier is not a summer accumulation type like glaciers to the east in the Himalaya. The retreat is similar to that of Samudra Tupa Glacier and Durung Drung Glacier.

Google Earth image from 2014 of Mount Kolahoi and its main glaciers flow directions indicated.

2001 Landsat image of Kolahoi Glacier

2015 Landsat image of Kolahoi Glacier

Google Earth image of the terminus area outlined in blue of Kolahoi Glacier in 2006 and 2014.

Image of the terminus of Kolahoi Glacier in 2010 from Jellani et al (2012)

North Cascade Winter Snowpack 2016, 33rd Field Season Approaches

On April 10, 2016May 2, 2024 By mspeltoIn glacier climate change, Glacier Observations, North Cascade Glaciers

This 2016 winter has proved much different than in 2015. In 2015 exceptional warmth led to record low snowpack despite above average precipitation. The warmth is illustrated using the North American Freezing Level Tracker for our Sholes Glacier site. The highest mean level by far is 2015, 500 m above average versus 180 m above average this winter. The low snowpack combined with a long warm melt season in 2015 led to the highest mass losses from North Cascade glaciers in our 32 years of observations.

Freezing Levels for the November-March period at Sholes Glacier in the North Cascades.

A key date for snowpack assessment has always been April 1. As a result there is good data set from six of the invaluable USDA SNOTEL sites in the North Cascades since 1946. A comparison of snowpack water equivalent (SWE) and total precipitation yield a ratio of SWE retained on April 1 to total precipitation. The result is the ratio between SWE and precipitation, snowpack storage efficiency has been in decline, as noted by Mote et al (2008) and Pelto (2008). The best long term precipitation stations in the region are Diablo Dam and Concrete, we use the average of the two. The storage efficiency ratio was a minimum in 2015 at only 19% of precipitation retained as snowpack. In 2016, 43% of precipitation has been retained leading to snowpack that is 10% above the mean for the 1984-2015 period.Winter precipitation over the period has a positive trend and SWE a negative trend. This declining ratio led Jon Riedel of the North Cascades National Park Service to observe that we now need 120% of average precipitation to achieve average snowpack. It is interesting to note that 2014, 2015 and 2016 had quite similar November-March total precipitation. With 2016 slightly exceeding 2014 for snowpack.

In 2014 the glaciers had a poor year, not due to low snowpack but to high melt season temperatures. What will transpire in 2016 will be the focus on our 33rd consecutive annual field season monitoring North Cascade glaciers. In the last 10 days warm weather in the region has led to significant snowpack melt. At low elevation sites snowpack depth and SWE have decreased by 20% at sites like Trinity 2930 feet. Just 10 miles away at Lyman Lake at 5980 feet the snow depth decreased from 170 inches to 142 inches, but SWE has not declined. As is typical this early snowmelt period leads to percolation and either refreezing or storage within the snowpack. This is still an important ripening that must occur before SWE can drop. Typically SWE reaches a maximum at the elevations of glaciers between May 1 and 10. A 10 day warm period as has occurred may indicate an early peak, but April could also feature more snow storms that will lead to future increases. From Alaska to British Columbia to Washington groups are heading into the field to assess snow depth on glaciers at the end of this winter season. Snowpits, snow stakes emplaced last last summer and Ground Penetrating Radar will all be deployed.

Trends in winter precipitation November-march in the North Cascades , average of Concrete and Diablo Dam. Mean SWE at six USDA SNOTEL station on April 1 (Fish Lake, Lyman Lake, Park Creek, Rainy Pass, Stampede Pass and Stevens Pass). Ratio of April 1 SWE and winter precipitation.

Mean SWE at six USDA SNOTEL station on April 1 (Fish Lake, Lyman Lake, Park Creek, Rainy Pass, Stampede Pass and Stevens Pass.

Assessing snow depth on Easton Glacier using crevasse stratigraphy.

Image above of Glacier Peak and below of Monte Cristo Peaks in the North Cascades on April 9, 2016 from a trip to Bedal Peak by raising3hikers at NWHikers.net. The blanket of snow remains deep.

Neumayer Glacier, South Georgia, 5.6 km retreat 1999-2016

On April 5, 2016May 2, 2024 By mspeltoIn glacier climate change, Glacier Observations, south georgia glacier retreat

Comparison of Neumayer Glacier in 1999 and 2016 Landsat images; red arrow indicates 1999 terminus locations, yellow arrows 2016 terminus locations. Purple arrows indicate upglacier thinning.

South Georgia sits amidst the circum Antarctic westerlies and its maritime climate leads to numerous glaciers. This region is famous for the endless march of storms parading around Antarctica . The island is south of the Antarctic Convergence, preventing any truly warm season from persisting. The cool glaciers covering a majority of the island and quite low equilibrium line altitudes. Neumayer Glacier is one of the largest tidewater glaciers on South Georgia. Sugden, Clapperton and Pelto (1989) noted the ELA of Neumayer Glacier at 550 m.

The BAS has a mapping function that provides glacier front positions since early in the 20th century. For Neumayer Glacier the 1938 position is 3.5 km down fjord from the 2006 position. There was essentially no retreat up to 1974 and limited retreat up to 1993. Gordon et al., (2008) observed that larger tidewater and sea-calving valley and outlet glaciers generally remained in relatively advanced positions until the 1980s. After 1980 most glaciers receded; some of these retreats have been dramatic.

Landsat Images from 1999 to 2016 indicates retreat of 5600 m from the red to the yellow arrow, this is 350 m/year. A glacier dammed lake along the north shore of the fjord no longer exists in 2016. The glacier appears to have retreated into a deeper section of the fjord then where it ended from 1970-2002. The glacier is on the verge of separation into two main tributaries. This will enhance calving from the glacier, and promote additional mass loss and retreat. This retreat will impact Konig Glacier to the north, which is connected to the Neumayer Glacier. Below the comparison of terminus location from 1989 to 2015 indicates a retreat of 6700 m. NASA Earth has piggy backed on this assessment, with excellent recent imagery. Calving rate increases with water depth. Calving rate increases with water depth and the degree of glacier flotation. Flotation depends on water depth, ice thickness and the number of pinning points. Pelto and Warren (1991) provided an expanded version of the water depth/calving relationship first quantified by Brown and others (1982). In the you would have never guessed it category, is the glacier retreat has been an aid to the rat population, as the glacier tongues used to corner populations.

BAS Glacier front map

Comparison of Neumayer Glacier in 1989 and 2015 Landsat images; red arrow indicates 1989 terminus locations, yellow arrows 2015 terminus locations.

New Zealand Glacier Change Index

On March 24, 2016May 2, 2024 By mspeltoIn glacier climate change, Glacier Observations, New Zealand glacier3 Comments

Terminus of Tasman, Mueller and Hooker Glacier terminus in Mount Cook 1972 map, no lake present.

Progalcial lakes forming in front of Tasman, Mueller and Hooker Glacier in 1990 above and 2015 Landsat images below.

Red arrows are the 1990 terminus and yellow arrows the 2015 terminus locations.

Overview

The Southern Alps of New Zealand are host to over 3000 glaciers that owe their existence to high amounts of precipitation ranging from 3 to 10 m (Chinn, 1999). The list below examines the changes of 12 glaciers examined in a separate post. The NIWA glacier monitoring program has noted that volume of ice in New Zealand’s Southern Alps has decreased by 36% with the loss of 19.0 km³ of glacier ice, from 53.3 km³ in 1978 to 34.3 km³ in 2014 (New Zealand Govt., 2015). Volume loss in New Zealand glaciers is dominated by 12 large glaciers (Salinger and Willsman, 2008). More than 90% of this loss is from 12 of the largest glaciers in response to rising temperatures over the 20th century (Chinn, 1999). In the 1972 map of the region there is no lake at the terminus of the Tasman Glacier, Mueller Glacier or Hooker Glacier; each are substantial in size by 2015. Each lake continues to expand and as glacier retreat continues .From 1977-2015 NIWA has conducted an annual snowline survey, in six of the last nine years the snowline has been significantly above average and three years approximately at the average (Willisman et al., 2015). This has driven the widespread glacier retreat underway. In each case the retreat of the largest glaciers has been enhanced by the formation and expansion of lakes, in this newly developing lake district. Dykes et al., (2011) identify the role of glacier lakes in accelerating the retreat of Tasman Glacier. The retreat of these glaciers has until recently been slowed by debris cover and the long low slope ablation zone segments (Chinn, 1999). Glaciers that lack debris cover and have a steeper slope have a more rapid response time, such as Fox Glacier and Franz Josef Glacier (Purdie et al., 2014). These two glaciers have been in the news of late due to rapid retreat causing glacier tours of the lower reaches of the glacier unsafe. NIWA reported that February of 2016 was the second warmest month of any month in New Zealand, which will drive snowlines higher and enhance glacier melt this year.

Many New Zealand glaciers are important for hydropower: Lake Tekapo and Lake Pukaki are both utilized for hydropower. Hooker Glacier, Mueller, Murchison and Tasman Glacier drain into Lake Pukaki, where water level has been raised 9 m for hydropower purposes. Water from Lake Pukaki is sent through a canal into the Lake Ohau watershed and then through six hydropower plants of the Waitaki hydro scheme: Ohau A, B and C. Benmore, Aviemore and Waitaki with a combined output of 1340 MW. Meridian owns and operates all six hydro stations located from Lake Pūkaki to Waitaki. The reduction of glacier area in the region will reduce summer runoff into Lake Pukaki and this hydropower system.

Gunn Glacier in, 2006 above and 2012 below,Google Earth image. Red arrows the 2006 terminus position yellow arrows 2012 terminus location. The glacier lost 25% of its area in six years.

Individual Glacier Posts

Murchison Glacier Tasman Glacier Balfour Glacier

Mueller Glacier Hooker Glacier Salisbury Snowfield

Lyell Glacier Douglas Neve Gunn Glacier

Upper Volta Glacier Donne Glacier

Donne Glacier from 2003-2012 in Google Earth images. Red arrow is the 2003 terminus and yellow arrow the 2012 terminus. A seven hundred meter retreat in a decade.

Alpine Glacier Mass Balance in 2015: Competes for Record Loss

On March 17, 2016May 2, 2024 By mspeltoIn climate change glacier retreat, glacier climate change, Glacier Observations1 Comment

Painting from Jill Pelto illustrating the Climate Change Data using multiple quantities: the annual decrease in global glacier mass balance, global sea level rise, and global temperature increase. The numbers on the left y-axis depict quantities of glacial melt and sea level rise, and the suns across the horizon contain numbers that represent the global increase in temperature, coinciding with the timeline on the lower x-axis.

The World Glacier Monitoring Service (WGMS) record of mass balance and terminus behavior provides a global index for alpine glacier behavior. The WGMS data set for terminus change contains 42 000 observations from 2000 glaciers extending from the mid-19th century. Annual mass balance is the annual change in volume due to snow and ice accumulation and snow and ice losses. Here, mass balance is reported in mm of water equivalent. The following analysis is something I work on annually as the United States Representative to the WGMS, putting the alpine glacier mass balance of the globe in perspective. Preliminary data for 2015 from 16 nations with more than one reporting glacier from Argentina, Austria, Canada, Chile, Italy, Kyrgyzstan, Norway, Switzerland, and United States indicate that 2015 will be the 36^th consecutive year of negative annual balances with a mean loss of −-1162 mm for 27 reporting reference glaciers and −1481 mm for 62 of all reporting glaciers (WGMS 2016). The number of reporting reference glaciers is 90% of the total whereas only 50% of all glaciers that will report have reported to date. When all data are available the 2015 mass balance will likely be comparable to 2003 the most negative year at −1268 mm for reference glaciers and −1198 mm for all glaciers.

The cumulative mass balance loss from 1980–2015 is 18.8 m, the equivalent of cutting a 20.5 m thick slice off the top of the average glacier. The trend is remarkably consistent from region to region (WGMS 2015). The decadal mean annual mass balance was −261 mm in the 1980s, −386 mm in the 1990s, -−727 mm for 2000s and −818 mm from 2010–15. The declining mass balance trend during a period of retreat indicates alpine glaciers are not approaching equilibrium and retreat will continue to be the dominant terminus response (Zemp et al. 2015). The recent rapid retreat and prolonged negative balances has led to many glaciers disappearing and others fragmenting (Pelto 2010; Carturan et al. 2013).

Annual glacier mass balance record of reference glaciers reporting to the WGMS.

In South America seven glaciers in Columbia, Argentina, and Chile reported mass balance. All seven glaciers had losses greater than −1200 mm, with a mean of −2200 mm. These Andean glaciers span 58°of latitude.

In the European Alps, mass balance has been reported for 14 glaciers from Austria, France, Italy, Spain and Switzerland. All 15 had negative balances exceeding −1000 mm, with a mean of −1860 mm. This is an exceptionally negative mass balance rivaling 2003 when average losses exceeded −2000 mm.

In Norway mass balance was reported for seven glaciers in 2015, all seven were positive with a mean of 860 mm. This is the only region that had a positive balance for the year. In Svalbard six glaciers reported mass balances, with all six having a negative mass balance averaging −675 mm.

In North America Alberta, British Columbia, Washington, and Alaska mass balance data from 17 glaciers was reported with a mean loss of −2590 mm, with all 17 being negative. This is the largest negative mass balance for the region during the period of record. From Alaska south through British Columbia to Washington the accumulation season temperature was exceptional with the mean for November–April being the highest observed.

In the high mountains of central Asia seven glaciers from China, Russia, Kazakhstan, and Kyrgyzstan reported data, all were negative with a mean of –705 mm.

Columbia Glacier, Washington in 2015 during our mass balance observations from the terminus and head of the glacier indicating the lack of snow cover retained and extensive melting,

Lago Onelli, Argentina trio of Glaciers Retreat and Separate

On March 10, 2016May 2, 2024 By mspeltoIn argentina glacier retreat, glacier climate change, Glacier Observations

Onelli Glacier (O), Belados Glacier (B) and Agassiz Glacier (A) compared in Landsat images from 1985 to 2016. The red arrow indicates the 1985 terminus location and yellow arrow is the 2016 terminus location.

The Onelli Glacier drains eastward from the South Patagonia Icefield (SPI) into Lago Onelli (LO), which then connects to Lago Argentino. Lago Onelli has three main glaciers terminating in the lake Agassiz (A), Onelli(O) and Bolados Glacier (B). Onelli glacier is noted as 13 km long with an area of 84 square kilometers by the Labratorio de Glaciologia in Chile . Davies et al (2012) noted that the most rapid period of retreat since 1890 for Bolado and Onelli Glacier was from 1986-2001. Warren and Sugden (1993) note an 1800 meter retreat from 1945-1992 for Onelli Glacier and 850 meters for Agassiz Glacier. Eric Shipton was the first to visit this glacier and did so in the company of Ohio State glaciologist John Mercer in 1958. They found Lago Onelli so filled with icebergs that little water could be seen (Shipton, Land of Tempest, 1963). Agassiz and Onelli Glacier were observed to have a shared terminus in 1958 much like Onelli Glacier and Belados Glacier in 1985.

A comparison of Landsat satellite images indicate the separation and retreat of Bolados (B) and Onelli Glacier (O) from 1985-2016. In 1985 the joint terminus cuts directly across Lago Onelli as one reasonably straight 1.6 km wide calving front just short of connecting with Agassiz Glacier. By 2004 the glacier had retreated 3000 m and Belados and Onelli were barely touching.The combined termini width was 1.8 km. By 2010 the glaciers were separated by 1300 meters. By 2016 Belados Glacier has retreated 3500 m from 1985-2016 and Onelli Glacier has retreated 3800 m. The glaciers in 2016 are separated from each other by 1800 m. The ELA in the satellite images from recent years has been 1300 meters. Agassiz Glacier has retreated 400 m during the 1985-2016 period. The glacier is grounded on three islands that acts as pinning points, reducing calving losses and the retreat rate.

Willis et al (2012) examined the mass change of the 12,100 km² SPI from 2000-2012: in the accumulation zone the average thickness change of −1.1 ± 0.1 m/year, for the ablation zone the average thickness change is −3.5 ± 0.02 m/year. This widespread loss even in the accumulation zone indicates that retreat will continue. A comparison of Landsat images from 1998 to 2013 indicates upglacier thinning at the purple arrows. Schaefer et al (2015) noted that the mass loss of SPI has been largely from increased calving losses. Mouginot and Rignot (2015) observed that Onelli Glacier does not have a high velocity reach extending beyond the immediate terminus zone, unlike major outlet glaciers of the SPI.

Google Earth image of Onelli Glacier and Belados Glacier in 2004 above and 2015 below. Orange arrow indicates the 2004 terminus location.

Landsat images from 1998 and 2013 indicating specific areas of upglacier thinning at the purple arrows.

Coronation Island Glacier Retreat, South Orkney Islands

On March 7, 2016May 2, 2024 By mspeltoIn Antarctic Glacier retreat, glacier climate change2 Comments

Lewis Glacier (S) and Sunshine Glacier (S) on Coronation Island in 1990 and 2015. Red arrow is 1990 terminus location and yellow arrow the 2015 terminus location.

Sunshine and Lewis Glacier are tidewater glaciers on the south side of Coronation Island in the South Orkney Islands. This is an area of excessive cloud cover leading to few available satellite images illustrating glacier change. A map of the glaciers from the British Antarctic Survey indicates they had nearly filled the embayments. The BAS maintains a research base on Signy Island (SG) that faces directly across the Orwell Bight to Sunshine Glacier. Coronation Island is extremely windy with the prevailing westerly wind averaging about 14 knots, at Signy Station with gales recorded on about 60 days each year. The Signy Station research focuses mainly on marine mammals and birds, with elephant seals, chinstrap, Adelie and gentoo penguins being most common.

Map of Coronation Island indicating Lewis Glacier (L), Sunshine Glacier (S) and the BAS Signy research station (SG)

View across Orwell Bight from Signy Island to Sunshine Glacier with the BAS Research vessel James Clark Ross in view during November 2015. (From BAS)

In 1990 Lewis Glacier had an east-west calving front extending from the last prominent east-west oriented ridge on the west side of the glacier. Sunshine Glacier extended well beyond the end of prominent ridge on the west edge of the glacier. By 2005 in the Google Earth image below Lewis Glacier had retreated in the center of the glacier more than on the west end. By 2013 Lewis Glacier had retreated to a second prominent east west trending ridge. Sunshine Glacier had retreated beyond the prominent ridge on the west by 2005. From 2005 to 2013 additional retreat occurred along the east side of Sunshine Glacier. The terminus on the east side of Sunshine Glacier is now adjacent to a series of nunataks comprising a ridge extending east from the glacier. Retreat of Lewis Glacier from 1980 to 2015 averaged 900 m across the 3 km wide calving front. Sunshine Glacier retreated 1100 m from 1990 to 2015 across the 3.5 km wide calving front. Both glaciers have relatively flat regions within one kilometer of the calving front which are prone to continued calving retreat. The glaciers are encased in sea ice much of the year protecting the calving front, but the summer climate is maritime with temperatures typically above freezing and the area relatively ice free. Today the region is also accessed by Oceanwide Expeditions. The retreat is similar to that of nearby on Endurance Glacier on Elephant Island and many retreating glaciers on South Georgia Island. .

Google Earth images from 2005 and 2013 indicating the 1990 (red arrows) and 2015 terminus locations (yellow arrows).

Click to access aca2_spa114.pdf

Jiongla Glacier, China Rapid Retreat 1988-2015

On March 3, 2016May 2, 2024 By mspeltoIn china glacier retreat, glacier climate change, Glacier Observations

Jiongla Glacier retreat right and Jiangyegong Glacier left retreat from 1988 to 2015 in Landsat images. The red arrow is the 1988 terminus and the yellow arrow the 2015 terminus. Jiongla Glacier retreated 3200 m and Jiangyegong Glacier 800 m.

Jiongla Glacier is at the northern boundary of the Brahmaputra River Basin at the east end of the Nyainqentanglha Shan. The glacier drains the western slopes of Koma Kangri Peak and ends in a lake before feeding into the Parlung Zangbo and then Yarlung Tsanpo. his glacier feeds the Parlung Zangbo which is the site of numerous planned hydropower projects, last image, before joining the Yarlung Tsanpo which becomes the Brahmaputra River. The Zangmu Dam went online in 2015, this hydropower facility will produce 2.5 billion kilowatt-hours of electricity a year. In a study by Tobias Bolch et al (2010) in the western Nyainqêntanglha Mountains glacier area decreased by 6% between 1976 and 2001 and continued to shrink from 2001–2009. Li et al (2010) examined glacier change over the last several decades in China and found ubiquitous glacier retreat and commonly lake formation as glaciers retreated. Ninglian and Shichang (2014) in the China National Report on Cryospheric Sciences noted a loss in glacier area of 15 to 17 % in the region. Here we examine satellite imagery from 1988, 2000, 2009, 2010, 2011 and 2015. The red arrow denotes the 1988 terminus and the yellow arrow the 2011 terminus.

In 1988 the lake where Jiongla Glacier ends is at 2 km long. By 2000 the glacier has retreated 1300 meters. In the 2003 terminus closeup that indicates vigorous flow through an icefall, purple arrow, 2 km behind the terminus. This indicates the lake will end before this point and the glacier does not have a substantial stagnant terminus tongue. By 2011 the lake is 4 km long, a 2 km retreat in 20 years. There are icebergs visible in the lake particularly in the 2003, 2009 and 2011 images indicating that this one a key reason for rapid recent retreat. In reviewing the satellite images for the region cloud cover made it difficult to find imagery near the end of the melt season. By 2015 the lake is 5200 m long indicating a 3200 m retreat from 1988-2015. The terminus is now within 500 of the increase in surface slope that suggests the end of the lake, and likely the end of the current rapid retreat. The 2011 image is from near the end of the melt season and indicates a snowline at 5150 m, blue dots, this is too high for equilibrium, with limited glacier area above 5500 m and the terminus at 4000 meters. This suggests that retreat will continue. The retreat here is similar to that of Thong Wuk Glacier and Requiang Glacier.

The neighboring Jiangyegong Glacier has experienced an 800 m retreat from 1988 to 2015. This terminus remains low slopes and heavily debris covered. The debris will slow the retreat, while the low slope indicates the lake can continue to expand enhancing retreat. This also suggests the rate of retreat will soon slow.T

Landsat image 2000 with the yellow arrow indicating the 2011 terminus position and the red arrow the 1988 terminus position.

2003 Google Earth Image

Landsat image 2011 with the yellow arrow indicating the 2011 terminus position and the red arrow the 1988 terminus position.

Hydropower dams completed, under construction and proposed.

Thong Wuk Glacier Terminus Tongue Collapse, China

On March 1, 2016May 2, 2024 By mspeltoIn china glacier retreat, glacier climate change, Glacier Observations

Thong Wuk Glacier comparison in 1988 and 2015 Landsat image. Red arrow is the 1988 terminus location, yellow arrow the 2015 terminus location and orange arrow indicates expanding lake of Yanglang Glacier.

There are two glaciers that drain the north side of Sepu Kangri Peak in the Eastern Nyainqêntanglha Mountains of Tibet in China. Thong Wuk to the east and Yanglang Galcier to the west. Most of the peaks in East Nyainqêntanglha Mountains are unclimbed, Sepu Kangri the highest peak was not climbed until 2002. The Sepu Kangri glaciers drain into the Salween River. In a study by Tobias Bolch et al (2010) in the western Nyainqêntanglha Mountains glacier area decreased by 6% between 1976 and 2001 and continued to shrink during the period 2001–2009. Li et al (2010) examined glacier change over the last several decades in China and found ubiquitous glacier retreat and commonly lake formation as glaciers retreated.

In this case we compare Landsat images from 1988, 2003, 2010 and 2015 and Google Earth images from 2011. In 1988 the lake at the end of the two glaciers are both 500-700 m long. By 2003 there is limited terminus change for the eastern side of the Thong Wuk terminus and the western side of the terminus has retreated 200 meters. By 2010 the terminus tongue is breaking up with many icebergs filling the lake. In 2011 the lake has expanded from a length of 600 meters in 1988 to 1300 meters. A closeup view in Google Earth of the eastern tongue indicates that this narrow tongue is not stable and the lake will lake quickly develop to an area of 1.7 km long and 0.8 km wide. In 2015 the glacier has retreated 1050 m since 1988, and the lake has an area of 2.4 square kilometers. Based on an increase in surface slope 500 m from the current terminus the lake will not expand more than this. This glacier remains heavily crevassed and has a vigorous accumulation zone indicating that it is not in danger of disappearing with current climate. In fact images from the first ascent of Sepu Kangri in 2002 indicate the annual layering in a crevasse, illustrating the considerable accumulation. The formation of lakes at the end of the glaciers as they retreat is quite common, including in the Tibetan glaciers.

Thong Wuk Glacier comparison in 2003 and 2010 Landsat image. Red arrow is the 2003 terminus location and orange arrow indicates expanding lake of Yanglang Glacier.

2011 Google Earth image. Note the heavy crevassing indicating considerable accumulation and flow.

2011 Google Earth image indicatint narrow tongue that has broken up by 2015.

Crevasse with annual layers on upper Thong Wuk Glacier from the Sepu Kangri Expedition in 2002.

Shamrock Glacier, Alaska Loses Terminus Tongue

On February 28, 2016May 2, 2024 By mspeltoIn alaska glacier retreat, glacier climate change, Glacier Observations, glaciers salmon

Shamrock Glacier comparison in 1987 and 2014 Landsat images. Red arrow 1987 terminus, yellow arrow 2014 terminus, purple arrows upglacier thinning and purple dots the snowline. The terminus tongues extending into the lake has been lost.

Shamrock Glacier flows north from the Neacola Mountains into Chakachamna Lake in the Lake Clark National Park of Alaska. This lake is transited by several species of salmon, mainly sockeye, heading into spawning areas upriver. The lake had been the site of a proposed hydropower plant, that would not have required building of a dam, but this project is currently not being developed. The National Park Service completed a Southwest Alaska Network mapping project that identified the changes of glaciers in the region. Lake Clark NP has 1740 glaciers which have lost 12% of their total area from 1950 to 2009 (Loso et al, 2014). Here we examine Landsat imagery from 1987 to 2014 to identify recent change of Shamrock Glacier.

July 2015 image looking across Shamrock Lake to Shamrock Glacier, taken by Jerry Pillarelli, note he has many more gorgeous images of area. The trimline on the far side of the glacier between sediment and vegetation indicates the 1950 margin. There is an elevation step several hundred meters inland of the terminus indicating Shamrock Lake will expand little.

In 1987 Shamrock Glacier had receded from a terminal moraine in Chakachamna Lake that it had terminated on in the 1950’s map. The new proglacial lake was less than 500 m across. The snowline was at 1200 m. In 2000 seen below the snowline was at 1350 m, and the terminus had narrowed more than it had retreated. By 2014 the terminus had retreated 900 m leaving the new Shamrock Lake within Chackachamna Lake. The new Shamrock Lake has an area of 4 square kilometers. This is the majority of the loss in glacier area since 1950 as well. In 2014 the snowline is quite high at 1450 m. A snowline that is consistently above 1300 m will drive continued retreat. Thinning upglacier is evident with expanded bedrock areas adjacent to the glacier margin above 1200 m at the purple arrows, indicating the snowline has been consistently higher than this. The retreat is similar to other glaciers in the region South Sheep Glacier, Sovereign Glacier and Fourpeaked Glacier. With the glacier retreating out of the lake basin soon, the rate of retreat should decline.

2000 Landsat image

2013 Image of Shamrock Glacier, Shamrock Lake and Chakachamna Glacier.

Mammoth Glacier, Wyoming Ongoing Retreat

On February 23, 2016May 2, 2024 By mspeltoIn climate change glacier retreat, glacier climate change, Glacier Observations

At top Landsat images from September 2013, 2014 and 2015 of Mammoth Glacier. The blue arrow indicates retained snowcover. A 2013 images of Mammoth Glacier from Sarah Meiser, note low slope and lack of crevassing above

Mammoth Glacier is in the Wind River Range of Wyoming. The ongoing retreat is leading to a glacier that does not warrant the name mammoth for size, but soon it will for obsolescence.The long and low sloped glacier is the largest west of the Continental Divide in the range. The glacier is at the headwaters of the Green River and Green River Lakes. The glacier had an area of 4 square kilometers in 1952, 2.1 square kilometers in 2007 and 1.8 square kilometers in 2015. The Landsat sequence above from 2013, 2014 and 2015 illustrates the problem, insufficient retained snowcover to approach equilibrium, that is also evident in 2006 shown below. The setting is better illustrated with images from Sarah Meiser who I think has the best collection of recent images of Wind River Glaciers. A glacier like Mammoth with limited avalanching needs more than 50% retained snowcover at the end of the summer (accumulation area ratio) to be in equilibrium. In 2013 with three weeks left in the melt season, the accumulation area ratio (AAR) is slightly below 50%, note Sarah Meisel image below. In 2014 the AAR is 25 % and in 2015 the AAR is 5-8%. These periods of sustained bare ice exposure lead to area loss and thinning. A comparison of Google Earth images illustrate the area loss. In each image the orange line is the 1966 map position, green line 1994 margin, blue line 2006 margin and purple line 2014 margin. The loss in area at the margin is evident as is the loss on the western side between 2006 and 2014. Retreat has been 200 m from 1966 to 1994, 95 m from 1994-2006 and 95 m from 2006 to 2014. Area loss after the poor snowcover in 2015 will continue and the glacier will not long be considered mammoth in size. Pelto (2010) examined glaciers in the Wind River Range and found two-thirds could not survive current climate as they did not have a persistent accumulation zone, including Mammoth Glacier and Sacagawea Glacier. Thompson et al (2011) noted a 38% loss in area of the 44 Wind River Range glaciers from 1966-2006. Maloof et al (2014) noted an even larger drop in volume of 63% of the same glaciers from 1966-2012.

Sarah Meiser image illustrating how close to the top of the glacier the bare ice extends. This fact indicates that all of the firn had been lost, thus the area shown has not been a recent accumulation area.