Retreat of Lake No Lake Glacier Junction, Juneau Icefield, British Columbia

Lake No Lake is a glacier dammed lake that periodically drains under the retreating Tulsequah Glacier. Canadian topographic maps indicate that three glaciers coalesced to fill this valley: Tulsequah, No Lake East and No Lake West. By 1984 when I had a chance to see this lake had formed while working on Tulsequah Glacier. Here we examine the retreat of the three glaciers that has led first to lake formation and now to a reduction in lake size from 1984-2013. nolake map In 1984 the lake extended to the terminus of No Lake East Glacier at the red arrow, after that glacier separated from the other two. Most of the valley below this point is filled with the Tulsequah and No Lake West Glacier that are still connected. The retreat of No Lake East is 1.75 km and now filled by a lake. A series of five Landsat 8 images from 2013 indicates the progression of this lake during a summer. On June 14, 2013 the No Lake East Glacier and Tulsequah Glacier are now separated with a valley 2.5 km long in between. This segment of the valley is filled by the lake, but the lake does not extend upvalley from West to East No Lake Glacier. By June 21 the lake has extended another 400 m upvalley to the northeast as the lake fills. By June 30th the lake has expanded to a length of 3 km and an average width of 600 m. By August 1st the lake has largely drained, though there are many icebergs still on the lake bottom and there is certainly some water remaining. By September 28th the lake is completely drained. The retreat of No Lake East Glacier from the 1984 terminus location at the red arrow is 450 m. The retreat of No Lake West Glacier from the yellow arrow is 400m. The 30 year retreat of the arm of the Tulsequah Glacier from the yellow to the pink arrow is 1800 m. As the damming arm of Tulsequah Glacier continues to thin this glacier will continue to decline in both depth and area. A 2010 Google Earth image is used to indicate the lake margin as indicated by stranded icebergs after drainage. Geertsema and Clague (2012) observed that this lake grew rapidly and began having glacier outburst floods during the 1970’s, but is now declining in size.nolake 1984
1984 Landat image

nolake 6142013
6-14-2013 Landsat image

6-21-2013 Landsat image

6-30-2013 Landsat image

nolake 812014
8-1-2013 Landsat image

nolake 9282013
9-28-2013 Landsat image

lake no lake 2010
Google Earth image, yellow dots lake outline

Tulsequah Glacier, British Columbia Jokuhlaups and Retreat

tulsequah glacier changeAbove is a paired Landsat image from 1984 left and 2013 right indicating the 2500 m retreat during this period of Tulsequah Glacier and formation of a new lake at the terminus. Tulsequah Glacier, British Columbia is a remote glacier draining from the Alaska-Canada boundary mountains of the Juneau Icefield. It is best known for its Jökulhlaups from lakes dammed by Tulsequah Glacier in northwestern British Columbia, Canada (Geertsema, 2000). This Tulsequah Glacier has retreated 1100 m since the Little Ice Age maximum in the 19th century. The continued retreat of the main glacier at a faster rate than its subsidiary glaciers raises the potential for an additional glacier dammed lake to form. The main terminus is disintegrating in a proglacial lake at present. This is not unlike the situation at the Gilkey Glacier just delayed. The images below are from Google earth in 2003 and 2007 and indicate the stagnant nature of the tongue in the lake, and lateral rifting that will be points of instability for a calving disintegration.
tulsequah terminus 2003

tulsequah terminus tongue 2007
As part of the Juneau Icefield Research Program We completed extensive snow pack measurements in the upper reach of the glacier in 1981-1984 and found that snow depths by summers end between 1800-2000 meters averaged 4-6 meters. These observations completed along a transect across the glacier noted in the image below, provide a good example of the different sensitivities of the glacier to global warming. In 1981 a warm winter led to minimal snowpack at lower elevations in the Juneau Region, however, the upper regions of the icefield had above average snowpack. Jabe Blumenthal and I observed snowpack of over 5 meters on the upper Tulsequah Glacier. The areas above 1500 m are not very sensitive to winter temperatures as most as precipitation will fall as snow. In 1982 Juneau had good snowpack and the upper portion of the icefield was gripped by extended cold, the minimum thermometer at Camp 8 registered -44 F. In the images below the ELA for 1984 (right) and 2006 is indicated by a black dotted line, our Camp * a green dot and our accumulation profile is an orange line. In 2006 (left) the ELA is quite high and the accumulation are not large enough for an equilibrium balance. In 1984 the ELA was lower and mass balance was positive.

Such cold conditions indicate continental dry climate conditions persisting. The result good snowpack low on the glacier and below normal snowpack high on the glacier. From Camp 8 Brian Hakala and I surveyed the upper Tulsequah and found 4 meters of snowpack. In 1984 the highest snowpack of 6 m was noted as Wilson Clayton and I again measured the upper Tulsequah. The glacier still had healthy accumulation. The issue driving the retreat is that the equilibrium line where melting equals accumulation and bare glacier ice is exposed has risen and is now typically at 1400 meters.
When water stored behind, on or under a glacier is released rapidly this outburst is referred to as a jökulhlaup. These outburst floods can pose a serious threat to life and property, but not from the modest floods of the Tulsequah system along this relatively undeveloped watershed. Tulsequah Glacier has a long history of often annual jökulhlaups since the early twentieth century documented by the USGS. The floods resulted after decades of downwasting and retreat of Tulsequah Glacier. In particular a tributary glacier feeding the Tulsdequah retreated and downwasted faster than the main glacier. This valley then was dammed by the main stem of the glacier. There is no surface drainage evident from either Lake No Lake or Tulsequah Lake (labelled TL and NN in image above), indicating all discharge is through a subglacial tunnel.the main stem of the glacier emerging at the terminus and causing modest downstream flooding. Each summer as the lake filled with meltwater, its area, level and volume would increase to the extent that the hydrostatic pressure would float the glacier enough to begin flowing, this water then would further melt the ice enlarging its conduit. Most of the release occurs within several days. Hydrologic data are used to reconstruct the times and peak discharges of floods from the glacier-dammed lakes The first jökulhlaups from Tulsequah Lake were the largest. The history of this these jökulhlaups has been declining peak and total discharges as the lake became smaller. Today, Tulsequah Lake is small, and it will disappear completely if Tulsequah Glacier retreats any further. From 1941-1971 Tulsequah Lake discharged annually. Since 1990 a Lake No Lake has been discharging annually. Lake No Lake), has formed and grown in size as Tulsequah Lake has diminished. Lake No Lake developed from a subglacial water body in a tributary valley, 7 km upglacier from Tulsequah Lake. Like Tulsequah Lake, Lake No Lake rapidly grew in area and volume during its youth, and in the 1970s it began to generate its own jökulhlaups. Lake No Lake appears to be following the same evolutionary path as Tulsequah Lake – its volume is now decreasing due to downwasting of Tulsequah Glacier, and its jökulhlaups are beginning to diminish. As Tulsequah Glacier continues to shrink in response to climatic warming, additional glacier-dammed lakes may form, renewing the cycle of outburst flood activity, the tributary where this is most likely is labeled Future New Lake in the final image.