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A jökulhlaup (or glacier burst) is a glacial outburst flood. It is an Icelandic term that has been adopted by the English language. It originally referred to the well-known subglacial outburst floods from Vatnajökull, Iceland which are triggered by geothermal heating and occasionally by a volcanic subglacial eruption, but it is now used to describe any large and abrupt release of water from a subglacial or proglacial lake/reservoir.
Since jökulhlaups emerge from hydrostatically-sealed lakes with floating levels far above the threshold, their peak discharge can be much larger than that of a marginal or extra-marginal lake burst. The hydrograph of a jökulhlaup from Vatnajökull typically either climbs over a period of weeks with the largest flow near the end, or it climbs much faster during the course of some hours. These patterns are suggested to reflect channel melting, and sheet flow under the front, respectively.[1] Similar processes on a very large scale occurred during the deglaciation of North America after the last ice age (e.g. Lake Agassiz), and presumably at earlier times, although the geological record is not well preserved.
Subglacial meltwater generation is one key to understanding of subglacial meltwater flow. Meltwater may be produced on the glacier surface (supraglacially), below the glacier (basally) or in both locations.[2][3] Ablation (surface melting) tends to result in surface pooling. Basal melting results from geothermal heat flux out of the earth, which varies with location, as well as from friction heating which results from the ice moving over the surface below it. Analyses by Piotrowski concluded that, based on basal meltwater production rates, the annual production of subglacial water from one typical north-western Germany catchment of 642x106 m3 during the last Weichselian glaciation.[4]
Meltwater may flow either above the glacier (supraglacially), below the glacier (subglacially/basally) or as groundwater in an aquifer below the glacier as a result of the hydraulic transmissivity of the subsoil under the glacier. If the rate of production exceeds the rate of loss through the aquifer, then water will collect in surface or subglacial ponds/lakes.[4]
The signatures of supraglacial and basal water flow differ with the passage zone. Supraglacial flow is similar to stream flow in all surface environments – water flows from higher areas to lower areas under the influence of gravity. Basal flow under the glacier exhibits significant differences. In basal flow the water, either produced by melting at the base or drawn downward from the surface by gravity, collects at the base of the glacier in ponds and lakes in a pocket overlain by hundreds of metres of ice. If there is no surface drainage path, water from surface melting will flow downward and collect in crevices in the ice, while water from basal melting collects under the glacier; either source can form a subglacial lake. The hydraulic head of the water collected in a basal lake will increase as water drains through the ice until the pressure grows high enough either to force a path through the ice or to float the ice above it.[2][5]
If meltwater accumulates, the discharges are episodic under Continental ice sheets as well as under Alpine glaciers. The discharge results when water collects, the overlying ice is lifted, and the water moves outward in a pressurized layer or a growing under-ice lake. Areas where the ice is most easily lifted (i.e. areas with thinner overlying ice sheets) are lifted first. Hence the water may move up the terrain underlying the glacier if it moves toward areas of lower overlying ice.[6] As water collects, additional ice is lifted until a release path is created.[7]
If no pre-existing channel is present, the water is initially released in a broad-front jökulhlaup which can have a flow front that is tens of kilometres wide, spreading out in a thin front. As the flow continues, it tends to erode the underlying materials and the overlying ice, creating a tunnel valley channel even as the reduced pressure allows most of the glacial ice to settle back to the underlying surface, sealing off the broad front release and channelizing the flow. The direction of the channel is defined primarily by the overlying ice thickness and second by the gradient of the underlying earth, and may be observed to "run uphill" as the pressure of the ice forces the water to areas of lower ice coverage until it emerges at a glacial face. Hence the configuration of the various tunnel valleys formed by a specific glaciation provides a general mapping of the glacier thickness when the tunnel valleys were formed, particularly if the original surface relief under the glacier was limited.[2][3]
The rapid high-volume discharge is highly erosive, as evidenced by the debris found in tunnels and at the mouth of tunnels, which tends to be coarse rocks and boulders. This erosive environment is consistent with creation of tunnels over 400 m deep and 2.5 km wide, as have been observed in the Antarctic.[2]
Piotrowski has developed a detailed analytic model of the process, which predicts a cycle as follows:
Whilst jökulhlaups were originally associated with Vatnajökull, they have been reported in the literature over a broad range of locations including the present day Antarctic, and there is evidence that they also occurred in the Laurentian ice sheet[8][9][10][11] and the Scandinavian ice sheet[12] during the last ice age.
In July 1994, an ice-dammed surface lake drained via a subglacial tunnel through Goddard Glacier, in the British Columbian Coast Mountains, resulting in a jökulhlaup. The flood surge of from 100 to 300 m3/second flowed 11 km through Farrow Creek to terminate in Chilko Lake, causing significant erosion. The ice dam has not reformed. Similar British Columbian jökulhlaups are summarized in the table below.[14]
| Lake name | Year | Peak discharge (m3/sec) | Volume (km3) |
|---|---|---|---|
| Alsek | 1850 | 30 | 4.5 |
| Ape | 1984 | 1600 | 0.084 |
| Tide | 1800 | 5,000-10,000 | 1.1 |
| Donjek | 1810 | 4000-6000 | 0.234 |
| Summit | 1967 | 2560 | 0.251 |
| Tulsequah | 1958 | 1556 | 0.229 |
As the Laurentide Ice Sheet receded from its maximum extent from around 21,000 to 13,000 years ago, two significant meltwater rerouting events occurred in eastern North America. Though there is still much debate among geologist as to where these events occurred, they likely took place when the ice sheet receded from the Adirondack Mountains and the St. Lawrence Lowlands.
Lake Agassiz was an immense glacial lake located in the center of North America. Fed by glacial runoff at the end of the last glacial period, its area was larger than all of the modern Great Lakes combined, and it held more water than contained by all lakes in the world today. It drained in a series of events between 13,000 BP and 8,400 BP.
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