RG150-17.01019 Glacier Retreat, Southern Patagonia Forms Lake

On November 21, 2016May 1, 2024 By mspeltoIn chile glacier melt, chile glacier retreat

Retreat of RG150 indicated in Landsat images from 1984, 2001 and 2015. Red arrow indicates 1984 terminus and yellow arrow 2015 terminus.

RG150 is a 3.5 km long glacier in Bernardo O’Higgins National Park on the western edge of the Southern Patagonia Icefield, Chile. RG150 is an unnamed glacier given this designation as part of the Randolph Glacier Inventory. The glacier terminates in a lake that drains into Seno Andrew. Willis et al (2012) observed that between February 2000 and March 2012 that the Southern Patagonia Icefield is rapidly losing volume and that thinning extends even to high elevations. The mass balance loss is occurring at a rate of −20.0 ± Gt/year, which is +0.055 mm/year of sea level rise. The retreat has been driven by increasing calving rates from the 1975-2000 to the 2000-10 period (Schaefer et al, 2015). The pattern of retreat is consistent between these glaciers and the region as noted by Davies and Glasser (2012), annual rates of shrinkage in the Patagonian Andes increased in from 0.10% year from 1870-1986, 0.14% year from 1986-2001, and 0.22% year from 2001-2011. Davies and Glasser (2012), note the all the glaciers in the complex inclusive of RG150 had their fastest retreat period from 2001-2015. Glasser et al (2016) observed both an increase in glacier proximal lakes and in debris cover on glaciers with glacier retreat from 1987-2015. These losses have led to retreat such as at Balmaceda Glacier, Glaciar Marconi and Glacier Onelli. Here we examine Landsat imagery from 1984 to 2015 to identify glacier change and the formation of a new lake.

In 1984 there was no glacier lake at the terminus, with the lower 1 km of the glacier being a low sloped glacier tongue. By 2001 a small proglacial lake had developed 250-300 m long. In 2005 the glacier retreat had led to continued lake expansion. The glacier had filled the lake with numerous small icebergs. By 2015 the glacier still terminates in the proglacial lake that is not 850-900 m long. The glacier retreat of 850 m since 1984 is 20-25% of the total glacier length. The low slope region is minimal in length in 2015 indicating the lake basin is almost complete. This will lead to a reduced rate of retreat. This is a very cloudy region, and the images here are not at the end of the melt season. Hence, the equilibrium line altitude can be ascertained. At the crest of the glacier 1300 m, there are a number of wind sculpted features that are 400-600 m long, attesting to the strong westerly winds in the region. RG150 has significant retained accumulation each year and can survive the current climate.

Retreat of RG150 indicated in Google Earth images from 2005 and 2015. Red arrow indicates 1984 terminus and purple arrows indicate wind features at the top of the glacier.

RG150 in Google Earth image looking upglacier in 2015. Red arrow indicates 1984 terminus and yellow arrow 2015 terminus and purple arrows indicate wind features at the top of the glacier.

Barnes Ice Cap, Baffin Island Evident Response to Climate Change

On November 18, 2016May 1, 2024 By mspeltoIn Canada glacier retreat1 Comment

Barnes Ice Cap transect and closeup of divide area in August 2016. Black dots indicate summit divide of the ice cap. Notice the channels extending away from the divide. These are not stream channels, as they are too wide, but they are meltwater formed valleys that are preferred pathways for the meltwater transport.

Barnes Ice Cap located in the center of Bafﬁn Island, Canada covers an area of ~5800 km2. The ice cap is approximately 150 km long, 60 km wide and has maximum ice thickness of ~730 m and a maximum ice elevation of 1124 m above sea level (asl) at the summit of the north dome (Andrews, 2002). They also note a retreat of the southeast margin of 4 m/year from 1961-1993 on the southeast margin (Jacobs et al 1997). Dupont et al (2012) identified that the melt season increased from 66 days fro the 1979-87 period to 87 days from 2002-2010. They also noted that ICESat altimeter data indicated the thinning of the BIC at a mean rate of 0.75 m/year for the 2003–2009 period. Gilbert et al (2016) Figure 5 indicates the ELA was at 950 in the 1960-80 period and is at 1100 m from 2002-2010 this leaves a limited accumulation zone area. observe that Barnes Ice Cap has nearly lost its accumulation area over the last 10 years, in part due to the longer melt season. The glacier does tend to not retain snowcover the accumulation zone consists of superimposed ice at the crest. Papasodoro et al (2016) noted that glacier wide balances were −0.52 m w.e./year from 1960 to 2013 and doubled to −1.06m w.e./year from 2005 to 2013. They also The drainage channel development suggests meltwater transport from versus refreezing of meltwater in 2016.

Landsat comparison of the northwest margin of the Barnes Ice Cap in 1990 and 2016. Red arrows indicate terminus locations in 1990. Purple arrows indicate an area of stream development parallel to the ice front. The bright area at the margin of the ice cap is Pleistocene ice (Andrews, 2002).

Here we examined Landsat imagery from 1990-2016 to illustrate the retreat of the northwest region of the icecap and to take a look at the 2016 melt features and lack of any retained snowcover on the ice cap. In 2016 the melt channels from the divide at the crest of the ice cap are impressive. There is no retained snowcover at the summit of the ice cap even on August 9th with several week left in the melt season. The melt pathways visible in the imagery from 2016 extend 10 km downslope from the crest of the icecap. In 1990 the ice cap terminated at the red arrows, this included contact with a peninsula in Nivlalis Lake and an island in Conn Lake. By 2011 and 2014 the glacier had retreated from the locations. In 2016 the total retreat of the margin has been 600 m at Nivalis Lake, 1100 m at the island in Conn Lake and 450 m further east at the red arrow halfway to Bieler Lake. This is a slow retreat rate compared to many glaciers, but represents a much higher rate than before 1990, with rates of 18-42 m/year. There is a new section of river parallel to the ice cap margin between Conn and Bieler Laker.

2011 Landsat image of northern margin indicating retreat from the 1990 postiion red arrows.

2014 Landsat image of northern margin indicating retreat from the 1990 postiion red arrows.

Hagafellsjokull, Iceland Reflects Langjokull Thinning & Retreat

On November 14, 2016May 1, 2024 By mspeltoIn glacier climate change, Glacier Observations, iceland glacier retreat

Landsat comparison of the terminus of Hagafellsjökull from 2000 and 2016. The red arrows are the 2000 terminus, the yellow arrows the 2016 terminus. Purple arrows indicate upglacier thinning.

Langjökull is the second largest iceap in Icalnd with an area of over 900 square kilometers. The mass balance of the icecap has been reported since 1997 and his lost over 1 m per year during this period (WGMS, 2016). Pope et al (2010) noted that the icecap has lost an area of 3.4 ± 2.5 km2 yr-1 over the decade from 1997-2007. Pope et al (2010) noted that the loss of ice volume confirms previously published predictions that Langjökull will likely disappear within the next 200 years if current trends continue. A key outlet of Langjökull is Hagafellsjökull which terminates in Hagvatn. Hagafellsjökull ended a sustained post Little Ice Age retreat in 1970. The ensuing advance of approximately 1 km ended by 2000. Here we examine Landsat imagery from 2000-2016 to identify recent changes in this outlet glacier.

In 2000 the glacier terminated on an island in Hagavatn, red arrow. The east margin of the glacier featured several locations where secondary termini overflowed a low ridge on the east side of the glacier. By 2006 the glacier had retreated 500-600 m from the island. By 2016 the terminus had retreated across its entire width by 800-850 m, 50 m/year, yellow arrows. A closeup view from the Iceland online map application illustrates the 2014 terminus red dots. The end of the glacier has a low slope, low velocity and is debris covered. The western side has terminated on land during this entire period and has approximately the same retreat rate as the eastern half that still ends in the expanding lake. There is little evidence of iceberg release into the lake, which helps explain the similar retreat rate. The low slope and upglacier thinning noted at the purple arrows indicate the retreat will continue. In 2014 the transient snowline reached near the head of the glacier at over 1100 m. In 2000, 2006 and 2016 the snowline with several weeks left in melt season ranged from 859-950 m. The retreat is similar to that of Norðurjökull another outlet of the Langjökull and Porisjokull.

Google Earth view of the terminus of Hagafellsjökull in 2014. Red arrow is the 2000 terminus position and yellow arrow the 2014 position.

Online Iceland Map Viewer indicating the terminus of Hagafellsjökull in 2014, red dots.

2006 and 2014 Landsat images of Hagafellsjökull indicating the transient snowline off the image in 2014 and at 850 m in 2006.

Thulagi Glacier, Nepal Retreat and GLOF Potential

On November 7, 2016May 1, 2024 By mspeltoIn Himalaya glacier retreat

Thulagi Glacier change in Landsat images from 1991 and 2016. Red arrow is 1991 terminus, yellow arrow 2016 terminus and purple arrow increasingly exposed bedrock rib amidst icefall.

Written With Prajjwal Panday: @prajjwalpanday

Thulagi Glacier terminates in a lake referred to both as Thulagi and Dona Lake. ICIMOD (2011) has identified this as a potential threat for a glacier lake outburst flood (GLOF) and has conducted extensive fieldwork there. Thulagi Lake is southwest of Mt..Manaslu in western Nepal at an altitude of 4,044 masl. Here we report on the identified threat and use Landsat imagery to identify changes in the glacier. Thulagi Lake has attracted much attention because two hydropower projects have been developed downstream on the Marsyangdi river basin, Marsyangdi Hydropower Project (69MW) and the Middle Marsyangdi Hydropower Project (70MW). Thulagi Lake began to form about 50 years ago and ICIMOD present field investigations showed that from 1995 to 2009, the length of Thulagi Lake had increased from 1.97 to 2.54 km, due to retreat and the lake area increased from 0.76 to 0.94 sq.km. ICIMOD (2011) did a bathymetric survey of Thulagi Lake using an inflatable boat. The volume was calculated to be 35.3 million cu.m in 2009 an increase from 31.75 million cu.m in 1995. The small increase despite significant area increase was because of a surface elevation lowering rate from 2003-2009 of 0.3 to 0.5 m/yr. They found the moraine walls were sinking, but more slowly at a rate of about 0.1 m/yr: The glacier experienced substantial retreat of 1.65 km from 1958 to 1995.

From 1991 to 2016 the glacier has retreated 750 m a rate of 30 m/year. The debris cover extends from the terminus 4.25 km upglacier to 4500 m. The low slope indicates the lake will continue to expand and the rate retreat should remain high. The bedrock rib is in the icefall that extends from 5600 m to 4600 m, purple arrow. The rock rib at 5000 m in the midst of the icefall is more exposed in Landsat images from 2012 to present than from 1988-2001. This suggests some thinning. All images indicate snowcover is persistent above 5800 m. The glacier terminus continues to calve into the lake as seen in the 2012 Google Earth Image, the 40 m high ice front calves only small icebergs that ICIMOD did not deem sufficiently large to trigger a GLOF event by the surge waves. They also noted that temporary blockage of the lake outlet by river ice, snow barriers, or lake ice debris, appears unlike.

Khanal et al (2015) examined the total value at risk under the modeled GLOF scenario of US $406.73 million for Thulagi. The estimated maximum flow was 4736 m3 /second for Thulagi. The majority of this potential damage was to the two hydropower projects. They noted 125 buildings and 100 acres of irrigated land at risk. A group of Nepali and US scientists carried out stability assessment of Thulagi Lake and its moraine after the April 2015 7.8 magnitude earthquake (USAID, 2015). They noted that the main moraine complex at the end of the lake is relatively stable (black arrow), while the end moraine is less stable (purple arrow). The earthquake caused some slumping of the outlet at the terminal moraine and some deterioration of this moraine. Overall the hazard due to the declining water level would offset some or all of this moraine deterioration in terms of overall risk of a GLOF. Although local people are aware of the deteriorating nature of the terminal moraine at Thulagi, community discussions revealed less concern regarding the possibility of an outburst flood (USAID 2015). However, there is a demand for risk reduction activities such as installation of early warning systems, lowering of lake levels, and development of community-based disaster response plans. There is a general consensus for a science-base community driven approach to address and find solutions for these types of lakes where communities and stakeholders participate starting from research to action.

The retreat of Thulagi Glacier is similar but less rapid than many Himalayan glaciers terminating in lakes; Thong Wuk, West Barun, Lumding and Lhonak

Middle Marsyangdi Hydropower Station and reservoir in Google Earth

Marsyangdi Hydropower Station and reservoir in Google Earth

Thulagi Lake outlet. Black arrow points to main moraine complex. Purple arrow to the less stable terminal moraine.

Thulagi Lake in 2012 Google Earth image. Yellow arrow is recently calved ice and purple arrow indicates bedrock within icefall.

Desolation Valley, Alaska, Conversion from Glacier to Lake

On November 1, 2016May 1, 2024 By mspeltoIn alaska glacier retreat, glacier climate change, Glacier Observations

Retreat of Desolation-Fairweather Glacier from 2010-2016 in Landsat images. The red arrow indicates 2010 terminus positions, yellow arrow the 2016 terminus. Pink arrow a delta exposed by lake level lowering. D=Desolation Glacier.

Desolation Glacier flows west from the Fairweather Range into Desolation Valley where in 1986 it joined with the Fairweather Glacier flowing from the north and the Lituya Glacier flowing from the south to fill the valley with glacier ice. This is no longer the case, the valley once known for its long relatively flat area of largely debris covered ice, is mostly a lake now. The valley has developed along the Fairweather Fault. Molnia (2007) noted that the tidewater termini of Lituya Glacier advanced ∼ 1 km since 1920 and continued to advance up to 2000 as it built an outwash plain reducing calving. Larsen et al (2015) noted thinning rates of 3 m per year for the Desolation Valley from Desolation Glacier north to Fairweather Glacier in the last decade (1994-2013). Alifu et al (2016) identified that Desolation Glacier and Fairweather Glacier have lost 2.6% and 2.2% of their glacier area, respectively from 2000-2012. Only minor surface area changes were seen in Lituya Glacier during this period. They also noted that the mean snow line altitude of Fairweather, Lituya and Desolation increased by 120–290 m. Since 2012 extensive ice loss of the Desolation-Fairweather complex has occurred. This is similar to the large rise in the transient snowline/equilibrium line noted by Pelto et al (2013) on nearby Brady Glacier.

In 1986 The Desolation Valley was filled with glacier ice from Fairweather Glacier to Liutya Bay. By 2010 the southern half of the valley from Lituya Glacier to the outlet of Desolation Glacier into the valley had opened up and the terminus of Desolation Glacier and Lituya Glacier were at the red arrows, this represented a 5.3 km section of glacier lost. In 2013 the northern half of the valley filled by the Desloation-Fairweather Glacier was breaking up but still ice filled. The Google Earth image from 2014 illustrates how broken up. By 2016 the collapse was total and the new terminus is at the yellow arrow a 5.5 km retreat since 2010, this is a loss of 6.5 square kilometers of ice. The lake level also dropped which led to exposure of a lacustrine delta that had been submerged in 2013 and 2014, pink arrow. The lake has expanded in area, but lost in mean depth. Will this continue to be a lake with continued retreat or become a braided river valley as the Fairweather Glacier continues to thin and retreat? Desolation Glacier is no longer calving and its retreat rate should slow. The terminus of the Fairweather Glacier should continue to retreat via calving in a fashion similar to glaciers around the world terminating in extensive lakes. Just to the north the North Fork Grand Plateau Glacier also experienced a large recent retreat with Landsat imagery in 2013 and 2014 indicating extensive calving from 2013 to 2015 and a retreat of 3.0 km, 1.5 km/year. Fingers Glacier is another nearby glacier that also is experiencing widespread retreat. More images of the region are in a field blog on the region.

Retreat of Desolation-Fairweather Glacier from 1986 and 2013 in Landsat images. The red arrow indicates 2010 terminus positions, yellow arrow the 2016 terminus. Pink arrow a delta exposed by lake level lowering. D=Desolation Glacier.

Google Earth image from 2014 of the disintegrating debris covered glacier.

Coley Glacier Retreat, James Ross Island, Antarctica

On October 28, 2016May 1, 2024 By mspeltoIn Antarctic Glacier retreat, climate change glacier retreat

Coley Glacier terminus comparsion in Landsat images from 2000 (red arrows) and 2016 (yellow arrow) indicating a retreat of 2 km along the western side and 1 km along the eastern side. Purple dots indicate the transient snowline and the purple arrow an area of debris exposed with glacier thinning.

Coley Glacier is a tidewater glacier on the northeast side of James Ross Island near the tip of the Antarctic Peninsula. Davies et al (2012) observed that 90% of the glaciers of the Northern Antarctic Peninsula including James Ross Island retreated from 1988-2001 and 79% from 2001-2009. They further observed that the rapid shrinkage of tidewater glaciers on James Ross Island would continue due to their low elevation and relatively flat profiles. Rohss Bay Glacier is one example of this having retreated 15 km from 1999-2009 (Glasser et al, 2011). Barrand et al (2013) note a strong positive and significant trend in melt conditions in the region, driving the retreat.

Coley Glacier in 2000 had a relatively straight calving front running across the embayment. The front represents the joining of four tributary glaciers. The snowline was generally below the top of the escarpment just west of Point C, the elevation of this lower glacier reach is below 200 m. This fits the low elevation low slope criteria noted by Davies et al (2012). By 2016 the glacier has developed a concave glacier front with the northern tributary almost separating the retreat ranges from 2 km on the west side to 1 km on the east side. The snowline is above the escarpment at 400 m. A comparison below of 2001 and 2015 indicates that the snowline in 2015 was also near 400 m and above the escarpment. A map of the region from the USGS (Ferigno et al.,2006) illustrates the retreat from the 1960’s to 2000. Nývlt et al (2010) reported on the retreat and changes on two glaciers on the north side of James Ross Island.

Coley Glacier terminus comparison in Landsat images from 2001 and 2015. Red arrows is the 2000 terminus and yellow arrows the 2016 terminus. Purple dots indicate the transient snowline and the purple arrow an area of debris exposed with glacier thinning.

COASTAL-CHANGE AND GLACIOLOGICAL MAP OF THE TRINITY PENINSULA AREA AND SOUTH SHETLAND ISLANDS, ANTARCTICA: 1843–2001

USGS (Ferigno et al.,2006)

Ross Ice Shelf Shear Zone-Research Focus of Gordon Hamilton

On October 25, 2016May 1, 2024 By mspeltoIn Glacier Observations

Satellite Image of the Shear Zone: The crevasses do have a surface representation, but are not generally open.

Gordon Hamilton lost his life on Saturday Oct. 22, 2016 conducting research in the shear zone between the Ross Ice Shelf and McMurdo Ice Shelf. I had the pleasure of working with and reviewing Gordon’s work; hence, it seems important to elaborate on the research that had brought researchers to this cold and hazardous corner of our planet.

Peter Rejcek of the Antarctic Sun provided an excellent context for this work two years ago. The Ross Ice Shelf is the world’s largest ice shelf at ~470,000 square kilometers. This floating ice shelf buttresses many faster flowing outlet glaciers that feed into it. Removal of the ice shelf would allow these glaciers to accelerate as has been seen after other ice shelves are lost, which could lead to enough drainage of the ice sheet to raise sea level 4 or 5 meters. The Ross Ice Shelf is in turn stabilized by pinning points. Such pinning points include Roosevelt Island and the shear zone. This shear zone represents a region of high shear and velocity change between the two ice shelves. Shear represents friction which helps pin the ice shelf. Gordon Hamilton was the principal investigator on a three-year project to map this shear zone and determine the mechanics. His hypothesis was without the shear zone the Ross Ice Shelf further south would slowly disintegrate. Without the ice shelf a glacier like Byrd Glacier which drains an immense area, 1,070,000 square kilometers, of East Antarctica could double its speed. Gordon was quoted by Peter Rejcek “The places that really control the future of the ice sheet are hard-to-access places, like shear margins or the underside of the ice shelf or the middle of crevassed outlet glaciers,” he added. “It’s hard to get good data sets there”. But that is exactly what he was continuing to do, getting the data that would us be able to model and forecast future behavior of the this region, which in turn is crucial to both the East and West Antarctic Ice Sheets.

Left: Landsat image of field area from Feb. 2016. Red arrows indicate shear zone.

Right: MODIS image from Oct. 23, 2016 illustrating the shear zone, red arrows.

To understand what was happening required detailed mapping of the crevasses within the shear zone. Gordon had noted that the sub-surface crevasses and the visible surface crevasses did not seem to match up well in 2014. This suggested an unusual flow pattern that could indicate instability within the shear zone. To examine and map the crevasses required detailed GPS and ground penetrating radar observations (GPR). Because of the danger a pair of Robot rovers were utilized that could do the bulk of the mapping. The robot rovers were developed by Jim Lever, a mechanical engineer with the U.S. Army Cold Regions Research and Engineering Laboratory (CRREL), in conjunction with the Thayer School of Engineering at Dartmouth College. The robots were used to prepare a safe route through the shear zone for the South Pole Traverse route and research in the area. In fact the two teams last week were camped close by and working together to identify and re-mediate crevasses on the route. Arcone et al (2016) noted that the lightweight robotic vehicles had towed the GPR equipment on 100 parallel transects over a 28 grid spanning the shear zone.

Some of their initial findings were presented at the AGU last fall (Kaluzienski et al, AGU, 2015). The GPR surveys had allowed detailed mapping of the internal structures of the Shear Zone. This identified crevasses both in the upper firn and in accreted marine ice at a depth of approximately 170 meters. They also found a spatial correspondence between near-surface and basal crevasses indicating that local lateral shear generated both. The distribution and orientation of the crevasses was consistent with predictions from a model. This suggests that the mismatch in crevasses that would suggest instability is not present. This work also indicates that high-resolution modeling can be used to predict the locations of basal crevassing which will lead to an improved understanding of ice-shelf mass balance processes. More images for the field area are in the field reports from Polartrec.

Deploying the robot on the ice shelf Photo Credit: Jim Lever

Insights on crevasses and what they could tell us about ice sheet behavior was a passion for Gordon. In Greenland he had been examining ways to use crevasse development to understand changing dynamics of tidewater outlet glaciers. The work conducted near Raven Camp after crevasses appeared in the skiway in 2012 was quite similar to the shear zone work in Antarctica. They installed stakes located with GPS including several continuously recording stations. This would allow determination of flow speed changes through the summer and if extensional flow had caused the formation of crevasse further inland. Understanding crevasses both for transportation needs and ice sheet behavior.

Crevasse Mapping in Greenland from a preliminary study with Gordon Hamilton- from Jill Pelto

Tasermiut Fjord, Greenland loses its Glacier Connection

On October 21, 2016May 1, 2024 By mspeltoIn glacier climate change, Glacier Observations, Greenland glacier retreat1 Comment

Landsat image sequence from 1999-2016. Red arrows mark the 1999 terminus, yellow arrows the 2016 terminus and the purple arrow a tributary that detaches from Semitsiaq (S). Tasermiut Sermeq (T) retreats from the fjord.

Tasermuit Fjord in southern Greenland is noted for its beauty, and until recently the fjord terminated at a glacier front. Currently no glacier reaches to the fjord. The retreat over the last two decades is similar to neighboring glaciers Kangersuneq Qingordleq and Qaleriq. The loss of direct glacier connection is also occurring at Alangordlia. Here we examine Landsat images from 1999-2016 to observe glacier change. At the head of the fjord is Sermeq Tasermiut and on the east side is Sermitsiaq.

In 1999 the Sermitsiaq Glacier terminated at the eastern end of a small lake, red arrow. Tasermiut Sermeq terminated in the fjord, red arrow. By 2002 Sermitsiaq had retreated from the lake, while Tasermiut Sermeq still reached the fjord. In 2013 Tasermiut Sermeq had retreated from the fjord and Sermitsiaq had retreated substantially from the lake and also had a significant tributary from the north detach, purple arrow. In 2016 Sermitsiaq has retreated 700 m since 1999, yellow arrow. Biggs (2011) had noted a 610 m retreat of the glacier from 1987-2009, a slower rate than since 1999. Tasermiut Sermeq has retreated 300 m since 1999,and has a narrow steep tongue that will melt back quickly in the near future.

Murray et al (2015) examined 199 tidewater glaciers in Greenland and noted significant retreat of 188 of them. This is changing fjord dynamics, which will in the case of Tasermiut affect the marine biology, which has not been studied in any detail yet. Students on Ice 2014 Arctic Expedition provides exceptional imagery of this fjord and the Nanotarlik region.

Google Earth imagery of the region. illustrating the loss of fjord connection after 2009.

Map of the region

Kangersuneq Qingordleq, Greenland Retreat Causes Separation

On October 18, 2016May 1, 2024 By mspeltoIn Greenland glacier retreat

Landsat comparison from 1999, 2001, 2013 and 2016 of Kangersuneq Qingordleq. Red arrow is 1999 terminus, yellow arrow is 2016 terminus. Purple dots mark the transient snowline and the purple arrow a detached tributary.

Kangersuneq Qingordleq is one of the most southerly tidewater glaciers in Greenland. It is a 15 km long glacier flowing from the mountains between Prince Christian Sound and Lindenow Fjord. It is more akin to an Alaskan tidewater outlet glacier than ice sheet fed Greenland outlet glaciers. Greenland tidewater outlet glaciers in this region have experienced substantial retreat since 1990, Weidick et al (2012) and Howat and Eddy (2011). Howat and Eddy (2011) examined 200 tidewater glaciers in Greenland from 2000 and 2010 observing that 191 had retreated, rapid retreat was observed in all sectors of the ice sheet. Moon and Joughin (2008) observed a synchronous ice sheet–wide increase in tidewater retreat from 2000–2006 versus 1992–2000, coincident with a 1.1°C increase in mean summer temperature. There was also an increased in sea surface temperature (Straneo et al, 2013). The retreat of glaciers in southern Greenland is changing the physical geography and hence physical oceanography of the fjords.

Here we examine Landsat imagery from 1999-2016 to identify recent behavior. In 1999 the glacier terminated at a narrow point in the fjord, red arrow. This location is also just beyond a junction with a tributary from the east. The fjord was just 600 m wide which would act as a pinning point restricting calving. It would not be surprising if fjord depth was also reduced here. By 2001 the glacier has retreated a short distance from the narrow point and is beginning to separate from the tributary. The transient snow line is at 950-1000 m. By 2005 the glacier had retreated 800 m and had fully separated from the eastern tributary, the ice front was 1 km wide. By 2013 the glacier has retreated into a section of the fjord that is 1.2 km wide and the transient snowline is at again at 950-1000 m. By 2016 the glacier has retreated 2.8 km since 1999. The transient snowline is 1000-1050 m in 2016, which is high enough to drive continued retreat. The fjord further widens to 1.4 km, 2.5 km behind the glacier front. This suggests that retreat will continue as there will be less sidewall stabilization. The glacier since 1999 has lost nearly 20% of its total length. To the northeast Qaleraliq has experienced a 3.2 km of its west arm and 1.2 km of its east arm from 1992 to 2012. To the northeast Tingmiarmiit Glacier retreat from 1999-2015 has led to complete separation of the western and northern tributary. The western tributary is the main glacier and has retreated 2.4 km and the northern tributary has retreated 2.2 km in the 16 year period. In the case of nearby Tasermiut Fjord retreat has led to fjord losing its tidewater connection.

Terminus of Kangersuneq Qingordleq in 2005 Google Earth image. Red arrow is 1999 terminus, yellow arrow is 2016 terminus.

Map of the region around Kangersuneq Qingordleq. Red arrow is 1999 terminus, yellow arrow is 2016 terminus.

2016 Field Season Results-North Cascade Glacier Climate Project

On October 14, 2016October 14, 2016 By mspeltoIn climate change glacier retreat, Glacier Observations, glaciers salmon

For Mount Baker, Washington the freezing level from January-April 20 was not as high as the record from 2015, but still was 400 m above the long term mean. April 1 snowpack at the key long term sites in the North Cascades was 8% above average. A warm spring altered this, with April being the warmest on record. The three-four weeks ahead of normal on June 10th, but three weeks behind 2015 record melt. The year was poised to be better than last year, but still bad for the glaciers. Fortunately summer turned out to be cooler, and ablation lagged. Average June-August temperatures were 0.5 F above the 1984-2016 mean and 3 F below the 2015 mean. The end result of our 33rd annual field season assessing glacier mass balance in the North Cascades quantifies this. Our Nooksack Indian Tribe partners again installed a weather and stream discharge station below Sholes Glacier.

The primary field team consisted of myself, 33rd year, Jill Pelto, grad student UMaine for the 8th year, Megan Pelto, Chicago based illustrator 2nd year, and Andrew Hollyday, Middlebury College. We were joined by Tom Hammond, NCCC President 13th year, Pete Durr, Mount Baker Ski Patrol, Taryn Black, UW grad student and Oliver Grah Nooksack Indian Tribe. The weather during the field season Aug. 1-17th was comparatively cool.

Mass Balance: Easton Glacier provides the greatest elevation range of observations. On Aug 2, 2016 the mean snow depth ranged from 0.75 m w.e. at 1800 m to 1.5 m w.e. at 2200 m and 3.0 m w.e. at 2500 m. Typically the gradient of snowpack increase is less than this. There was a sharp rise in accumulation above 2300 m. This is the result of the high freezing levels. The mass balances observed fit the pattern of a warm but wet winter. The high freezing levels left the lowest elevation glaciers Lower Curtis and Columbia Glacier with the most negative mass balance of approximately 1.5 m. The other six glaciers had negative balances of -0.6 to -1.2 m. This following on the losses of the last three years has left the glaciers with a net thinning of 6 m, which on glaciers averaging close to 50 m is a 12% volume loss in four years. We anticipate with that this winter will be cooler and next summer the glaciers happier. We will back to determine this.

Snowpack loss from Aug. 5-Sept. 22 is evident in the pictures below on Sholes Glacier. Detailed snow depth probing, 112 measurements, of the glacier on August 5th allows determination of ablation as the transient snow line traverses probing locations from Aug. 5. GPS locations were recorded along the edge of blue ice on each of the dates. Ablation during this period was 2.15 m.

Terminus Change: We measured terminus change at several glaciers and found that a combination of the 2015 record mass balance loss and early loss of snowcover from glacier snouts in 2016 led to considerable retreat since August 2015. The retreat was 25 m on Easton Glacier, 20 m on Columbia Glacier, 20 m on Daniels Glacier, Sholes Glacier 28 m, Rainbow Glacier 15 m, Lower Curtis Glacier 15 m. The main change at Lower Curtis Glacier was the vertical thinning, in 2014 the terminus was 41 m high, in 2016 the terminus seracs were 27 m high. The area loss of the glaciers will continue to lead to reduced glacier runoff. We continued to monitor daily flow below Sholes Glacier which allowed us to determine that in August 2016 45% of the flow of North Fork Nooksack River came from glacier runoff. This is turns has impacts for the late summer and fall salmon runs.

Shatter & Shudder Glacier Retreat, British Columbia Lakes Form

On October 11, 2016May 1, 2024 By mspeltoIn Canada glacier retreat, glacier climate change, Glacier Observations, Uncategorized

Red arrow is the 1985 terminus location and yellow arrow the 2016 terminus location. Note the formatiion of new lakes at end of both glaciers. Purple dots is the transient snowline in August of each year.

Shatter and Shudder Glacier are at the eastern end of the Spearhead Range in Garibaldi Provincial Park, British Columbia. Osborn et al (2007) mapped the Little Ice Age extent of the glaciers compared to the 1990’s margins indicating a retreat of 300 m for Shatter Glacier and 700 m for Shudder Glacier (see below). Koch et al (2009) identified the recession in area from 1928 to 1987 noting a 6% loss in Shatter Glacier and 22% loss for Shudder Glacier. Koch et al (2009) identify an 18% loss in area from 1987-2005, indicating considerable recent change in the Park. Here we use Landsat imagery from 1985-2016 to update glacier change.

In 1985 there are no lake at the terminus of either Shatter or Shudder Glacier. In 2002 a lake has formed at the terminus of Shudder Glacier, but not Shatter Glacier. In 2016 both glaciers have proglacial lakes that have formed, and the terminus of both glaciers have retreated from the lakes. This marks a retreat of 325 m on Shudder Glacier and 275 m on Shatter Glacier since 1985. Shudder Glacier retreated more rapidly in the first half of this period, while Shatter Glacier has experienced most of the retreat since 2005.

On Shatter and Shudder Glacier In 1987 the late August image indicates the snowline is at 2040 m, in mid-August 2015 the snowline is at 2250 m. In late August of 2014 the snowline was at 2120 m. In mid-August 2016 the snowline is at 2080 m. The higher snowlines are an indicator of mass loss for these glaciers that in turn drives retreat. The region continues to experience significant loss in glacier area and development of many new alpine lakes with glacier retreat, five new lakes since 1987 just in this range with seven glaciers. Spearhead and Decker Glacier are two other glaciers in the range that have developed new lakes since 1987. Nearby Helm Glacier is faring even worse.

Landsat images from 1987, 2014 and 2015 indicating the transient snowline position at the purple dots on Shatter and Shudder Glacier.

Pink Arrows indicate five new alpine lakes that have developed since 1987 as Spearhead Range glaciers have retreated

Map of Spearhead Range glacier extent for LIA-Bold lines and 1987, light lines from Osborn et al (2007)

Findelengletscher, Switzerland Retreat & Hydrology Insights from David Collins

On October 3, 2016May 1, 2024 By mspeltoIn glacier climate change, switzerland glacier retreat

Landsat image comparison of Findelengletscher from 1988 to 2015. Red arrow indicating the 1988 terminus location and yellow arrow the 2015 terminus location. The purple arrows indicate two tributaries connected to the main glacier in 1988 and now disconnected.

Findelengletscher along with Gornergletscher drains the west side of the mountain ridge extending from Lyskamm to Monte Rosa, Cima di Jazzi and Strahlhorn in the Swiss Alps. It is the headwaters of the Matter Vispa. This glacier was also the favorite field location for David Collins, British Glaciologist/Hydrologist from University of Salford who passed away last week. David had a wit, persistence and insight that are worth remembering. This post examines both David’s findings reaching back to the 1970’s gained from a study of glaciers in this basin and changes of the glacier since 1988 as evident in Landsat images. Findelengletscher drains into the Vispa River which supports for hydropower project, with runoff diverted into two hydropower reservoirs, Mattmarksee operated by the Kraftwerke Mattmark producing 650 Gwh annually, and Lac de Dix operated by Grande Dixence that produces 2000 Gwh annually. There are two smaller run of river projects as well.

The Swiss Glacier Monitoring Network has monitored the terminus change of Findelengletscher since the 1890’s. The glacier advanced 225 m from 1979-1986, retreated 450 m from 1988-1999 and retreated 850 m from 1999-2015. This is illustrated above with the red arrow indicating the 1988 terminus location and the yellow arrow the 2015 terminus location. The purple arrows indicate two tributaries connected to the main glacier in 1988 and now disconnected. The more limited retreated from 1988-1999 is evident in images below. The retreat is driven by mass losses with Huss et al (2012) noted as 1 m/year in the alps from 2001-2011. The snowline has typically been above 3250 m too high for equilibrium in the last decade. Melt at the terminus has typically been 7-8 m (WGMS).

Collins (1979) in work funded through hydropower looked at the chemistry of glacier runoff and found that glacier meltwater emerging in the outlet stream was enriched in Calcium, Magnesium and Potassium in particular versus non-glacier runoff, this led to a much higher conductivity. Collins (1982) noted the reduction in streamflow below Gornergletscher from summer streamflow events that reduced ablation for up to a week after the event. Collins (1998) noted that a progressive rise of the transient snow line in summer increases the snow-free area, and hence the area of basin which rapidly responds to rainfall. Rainfall-induced floods are therefore most likely to be largest between mid-August and mid-September and in this period of warmer temperatures and higher snowlines. Collins (2002) Mean electrical conductivity of meltwater in 1998 was reduced by 40%. In the same 60 day period in 1998, however, solute flux was augmented by only 2% by comparison with 1979. Year-to-year climatic variations, reflected in discharge variability, strongly affect solute concentration in glacial meltwaters, but have limited impact on solute flux. Collins (2006) identified that in highly glacier covered basins, over 60%, year-to-year variations in runoff mimic mean May–September air temperature, rising in the warm 1940s, declining in the cool 1970s, and increasing by 50% during the warm dry 1990s/2000s. In basins with between 35–60% glacier cover, flow also increased into the 1980s, but declined through the 1990s/2000s. With less than 2% glacier cover, the pattern of runoff was inverse of temperature and followed precipitation, dipping in the 1940s, rising in the cool-wet late 1960s, and declining into the 1990s/2000s.. On large glaciers melting was enhanced in warm summers but reduction of overall ice area through glacier recession led to runoff in the warmest summer (2003) being lower than the previous peak discharge recorded in the second warmest year 1947. Collins (2008) examined records of discharge of rivers draining Alpine basins with between 0 and ∼70% ice cover, in the upper Aare and Rhône catchments, Switzerland, for the period 1894-2006 together with climatic data for 1866-2006 and found that glacier runoff had peaked in the late 1940s to early 1950s.

These observations have played out further with warming, retreat and more observations. Finger et al (2012) examine the impact of future warming on glacier runoff and hydropower in the region. They observe that total runoff generation for hydropower production will decrease during the 21st century by about one third due glacier retreat. This would result in a decrease in hydropower production after the middle of the 21st century to keep Mattmarksee full under current hydropower production. Farinotti et al (2011) noted that the timing of maximal annual runoff is projected to occur before 2050 in all basins and that the maximum daily discharge date is expected to occur earlier at a rate of ~4 days/decade. Farinotti et al (2016) further wondered if replacing the natural storage of glacier in the Alps could be done with more alpine storage behind dams.

Google Earth image indicating flow of the Findelengletscher.

Landsat image comparison of Findelengletscher from 1999 to 2016. Red arrow indicating the 1988 terminus location and yellow arrow the 2015 terminus location. The purple arrows indicate two tributaries connected to the main glacier in 1988 and now disconnected.