Map showing distribution of moraines and extent of glaciers from the mid-19th century to 1979 in the Mount Jackson area, Glacier National Park, Montana
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Late 19th century
Glacier mass balance
Beach morphodynamics
Deglaciation
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Terminal moraine
Glacier mass balance
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Mount
Late 19th century
Glacier mass balance
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Abstract. Topographic development via paraglacial slope failure (PSF) represents a complex interplay between geological structure, climate, and glacial denudation. Southeastern Tibet has experienced amongst the highest rates of ice mass loss in High Mountain Asia in recent decades, but few studies have focused on the implications of this mass loss on the stability of paraglacial slopes. We used repeat satellite- and unpiloted aerial vehicle (UAV)-derived imagery between 1990 and 2020 as the basis for mapping PSFs from slopes adjacent to Hailuogou Glacier (HLG), a 5 km long monsoon temperate valley glacier in the Mt. Gongga region. We observed recent lowering of the glacier tongue surface at rates of up to 0.88 m a−1 in the period 2000 to 2016, whilst overall paraglacial bare ground area (PBGA) on glacier-adjacent slopes increased from 0.31 ± 0.27 km2 in 1990 to 1.38 ± 0.06 km2 in 2020. Decadal PBGA expansion rates were ∼ 0.01 km2 a−1, 0.02 km2 a−1, and 0.08 km2 in the periods 1990–2000, 2000–2011, and 2011–2020 respectively, indicating an increasing rate of expansion of PBGA. Three types of PSFs, including rockfalls, sediment-mantled slope slides, and headward gully erosion, were mapped, with a total area of 0.75 ± 0.03 km2 in 2020. South-facing valley slopes (true left of the glacier) exhibited more destabilization (56 % of the total PSF area) than north-facing (true right) valley slopes (44 % of the total PSF area). Deformation of sediment-mantled moraine slopes (mean 1.65–2.63 ± 0.04 cm d−1) and an increase in erosion activity in ice-marginal tributary valleys caused by a drop in local base level (gully headward erosion rates are 0.76–3.39 cm d−1) have occurred in tandem with recent glacier downwasting. We also observe deformation of glacier ice, possibly driven by destabilization of lateral moraine, as has been reported in other deglaciating mountain glacier catchments. The formation, evolution, and future trajectory of PSFs at HLG (as well as other monsoon-dominated deglaciating mountain areas) are related to glacial history, including recent rapid downwasting leading to the exposure of steep, unstable bedrock and moraine slopes, and climatic conditions that promote slope instability, such as very high seasonal precipitation and seasonal temperature fluctuations that are conducive to freeze–thaw and ice segregation processes.
Denudation
Glacier mass balance
Glacier morphology
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ABSTRACTABSTRACTThe extensive occurrence of glacier ice cores to landforms and deposits of the Neoglacial and Little Ice Age periods in the St. Elias Mountains of the southwest Yukon is described. These glacier ice cores were produced during active glaciation and have been preserved, in locations such as the Donjek Glacier moraine, for over 500 years. Incorporation of ice in landforms and deposits occurs during glacier surges, glacier advance or glacier backwasting as well as during stagnation of the glacier. The primary terrain ranges from sequences of moraines, providing a detailed record of glacier fluctuations, to ice contact landforms. The degradation of the ice-cored terrain is controlled by hydrological and glaciological processes, which expose the ice core, rather than by melt beneath the surficial materials.
Glacier morphology
Landform
Cirque glacier
Ice core
Glacier mass balance
Tidewater glacier cycle
Rock glacier
Glacier ice accumulation
Glacial landform
Terminal moraine
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An inventory of glacier lakes was compiled based on observations carried out for 30 glacier lakes in the northern and northwestern parts of Bhutan in autumn 1998. Risk assessments for glacier lake outburst floods were made for these glacier lakes. Historical variations of glacier lakes and glacier termini were examined using photographs, satellite images, maps and published observations. In the northern region of Bhutan, supraglacial ponds on some debris-covered glaciers in the 1950s have subsequently grown into moraine-dammed lakes. Also, proglacial lakes have expanded substantially as a result of retreat of glacier termini.
Tidewater glacier cycle
Glacier mass balance
Cirque glacier
Rock glacier
Glacier morphology
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Thinning
Tidewater glacier cycle
Glacier mass balance
Rock glacier
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It is well known that glaciers in Europe have been remarkably retreating in recent period according to the climatic change. Roseg and Tschierva Glacier, descending northwest slope of Mt. Bernina (4, 049 m), eastern Swiss Alps, as a typical valley glacier system, is one of the example.The author had a chance in his cartographic research at Zurich Technical University (ETH) to compile a topographical map of glacier, using the aerial photographs taken by Swiss Federal Topographic Survey (Eidge. Landestopographie) in 1971, and to compare it with the other topographical maps which are showing glacial conditions in 1934, 1955 and 1964 respectively.As the result of comparison, it is recognized that the ice tongue of Roseg Glacier has been retreated about 1, 000 m in 37 years from 1934 to 1971, while the ice tongue of Tschierva Glacier has been retreated about 800 m in the same period.Behind the retreated Tschierva glacial tongue, undulating features of ground moraine are left in the form of river terraces according to the erosion by melted water. Lateral moraines at the both sides of the glacier have been built up as remarkable dykes with steep slopes and knife ridges, they have been, however, suffered from vigorous gully erosion on their slopes after the retreat of ice tongue. As the result of erosion, location of knife ridges were shifted outward. Especially on the left dyke the shift of ridge was reached about 70 m.Since this left dyke of lateral moraine had been built as a huge crossing barrier over Roseg glacial valley, a large glacial lake was formed in Roseg valley in consequence of dam up of melted water from the glacial tongue.In Tschierva glacial valley, half ring shaped features of old terminal moraine are recognized at the altitude of 2060 to 2070 m. According to Professor E. Spiess's opinion, these features have been formed by old glacial tongue in 1850 and are covered by bushes of Rhododendron juniperus nana. While on the ground moraine there are scarcely recognized vegetations on the aerial photographs taken in 1971. These facts perhaps show that the retreat of Tschierva Glacier amount to about 1, 000 m during the period from 1850 to 1971 has been occured not gradually and continuously but suddenly after relatively long stable period. The author considers that the retreat of about 800 m, which is the greater part of total volume has been occured in recent 37 years.On both mountain slopes of Roseg Glacier there are old moraine terraces which have been built in Ice Age. They keep still flat surfaces but their flanks present singular sight of badland and supply large quantity of detritus to make talus scarp.Two block-stream features are recognized on the gentle slope of Mt. Aguagliouls.They are considered as successors of former ground moraines.The author would like to thank Prof. E. SPIESS, Associate Prof. Ch. HOINKES and Mr. F. FURRER in Zurich Technical University for their guidance and assistance. And he is also indebted to Swiss Federal Topographic Survey for the permission to reproduce topographical map and aerial photographs.
Glacier morphology
Ice tongue
Cirque glacier
Tidewater glacier cycle
Glacier mass balance
Accumulation zone
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In Mount Kawa Karpo,the variation of glaciers,as well as the correlation between glaciers and climate change,is rarely known,because there is lack of data about spatial and temporal variation of glaciers,and less research about the variation has been done.Dendrochonology is a world-famous tool to reconstruct glacier fluctuation.In this study,the tree-ring samples from the moraine by the glacier terminus are analyzed,and then variation of the Melang Glacier in the past 40 years is determined by means of topographic map and latest GPS boundaries in GIS.Using the dendrochronology,the age of Picea likiangensis living on the moraine by the glacier terminus and the forming age of the moraine are determined.It is found that the latest event about glacier variation occurred in 1987,after a topographic map being completed in 1971.Derived from the ages of spruces living inside and outside the moraine,it is believed that from 1987 to 1993 the glacier terminus had existed stably at the position where spruces begun to grew in 1998.Because the youngest tree has grown,it is inferred that the glacier retreated about 1993.There is a glacier close to the Melang Glacier,whose terminus was thought at the steady state until 1959,and in the GIS map of 1971,the glacier terminus is outside the area where trees live.
Glacier terminus
Tidewater glacier cycle
Glacier mass balance
Accumulation zone
Glacier morphology
Terminal moraine
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Terminal moraine
Glacial landform
Landform
Crevasse
Tidewater glacier cycle
Meltwater
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Abstract “Avalanche-type” medial moraines are described on four Torngat Mountains glaciers with single, rather than compound, firn basins. They form from debris avalanching down couloirs and are exposed by ice melt to form extensive debris covers on glacier snouts in the Torngat Mountains. The debris may play an important part in helping the glacier survive periods with warm summers and/or dry winters since, in the Torngat Mountains, average ice melt on debris-covered sites is approximately one-third that on exposed ice.
Firn
Glacier morphology
Terminal moraine
Glacier mass balance
Rock glacier
Glacier ice accumulation
Tidewater glacier cycle
Ice caps
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