query: what type of glacier forms a u shaped valley

pos: U-shaped valley U-shaped valley U-shaped valleys, trough valleys or glacial troughs, are formed by the process of glaciation. They are characteristic of mountain glaciation in particular. They have a characteristic U shape, with steep, straight sides and a flat or rounded bottom (by contrast, valleys carved by rivers tend to be V-shaped in cross-section). Glaciated valleys are formed when a glacier travels across and down a slope, carving the valley by the action of scouring. When the ice recedes or thaws, the valley remains, often littered with small boulders that were transported within the ice, called glacial till or glacial erratic. Examples

pos: U-shaped valley that it could be responsible for the severe carving of bedrock characteristic of glacial erosion. German geologist Penck and American geologist Davis were vocal supporters of this unprecedented glacial erosion. Progress was made in the 1970s and 1980s on the possible mechanisms of glacial erosion and U-shaped valleys via models proposed by various scientists. Numerical models have been created to explain the phenomenon of carving U-shaped valleys. Pazynych V. "Origin of U-shaped valleys" U-shaped valley U-shaped valleys, trough valleys or glacial troughs, are formed by the process of glaciation. They are characteristic of mountain glaciation in particular. They have a

neg: Reintal (Wetterstein) Reintal (Wetterstein) The Reintal ("Rein Valley") is the name given to the upper and lower valleys of the River Partnach between the "Zugspitzplatt" plateau and the Partnachklamm gorge. A hiking route to Germany's highest mountain, the Zugspitze runs through the valley. The valley was formed during the Würm Ice Age by the Reintal Glacier and then deepened by the Partnach in the post-ice age period after the retreat of the glacier to the periphery of the Schneefernerkopf mountain. The upper Reintal, which was shaped by the glacier and today forms a U-shaped glacial valley, ends between the "Hohe Gaifkopf" in

neg: Pamir Mountains Xiao'erjing: پَامِعَر or ڞوْلٍْ. The name "Pamir" is used more commonly in Modern Chinese and loaned as . According to Middleton and Thomas, "pamir" is a geological term. A pamir is a flat plateau or U-shaped valley surrounded by mountains. It forms when a glacier or ice field melts leaving a rocky plain. A pamir lasts until erosion forms soil and cuts down normal valleys. This type of terrain is found in the east and north of the Wakhan, and the east and south of Gorno-Badakhshan, as opposed to the valleys and gorges of the west. Pamirs are used for

neg: Valley are hanging. The brooks flow into the river in form of deep canyons or waterfalls. Usually this fact is the result of a violent erosion of the former valley shoulders, a special genesis found also at arêtes and glacial cirques, at every Scottish glen, or in a northern fjord. A hanging valley is a tributary valley that is higher than the main valley. They are most commonly associated with U-shaped valleys when a tributary glacier flows into a glacier of larger volume. The main glacier erodes a deep U-shaped valley with nearly vertical sides while the tributary glacier, with a

neg: U-shaped valley of U-valleys are found in mountainous regions like the Alps, Himalaya, Rocky mountains, Scottish Highlands, Scandinavia, New Zealand and Canada. A classic glacial trough is in Glacier National Park in Montana, USA in which the St. Mary River runs. Another famous U-shaped valley is the Nant Ffrancon Valley in Snowdonia, Wales. Formation of a U-shaped valley happens over geologic time, meaning not during a human’s lifespan. It can take anywhere between 10,000 and 100,000 years for a V-shaped valley to be carved into a U-shaped valley. These valleys can be several thousand feet deep and tens of miles long. Glaciers

neg: Valley bottom. In Southern England, vales commonly occur between the escarpment slopes of pairs of chalk formations, where the chalk dome has been eroded, exposing less resistant underlying rock, usually claystone. Rift valleys, such as the Albertine Rift, are formed by the expansion of the Earth's crust due to tectonic activity beneath the Earth's surface. There are various forms of valley associated with glaciation that may be referred to as glacial valleys. A valley carved by glaciers is normally U-shaped and resembles a trough. This trough valley becomes visible upon the recession of the glacier that forms it. When the ice

neg: U-shaped valley deposited by the glacier. A glacial trough or glaciated mountain valley often ends in an abrupt head known as the 'trough end' or 'trough head'. This may have almost sheer rock walls and spectacular waterfalls. They are believed to have been formed where a number of small glaciers merge to produce a much larger glacier. Examples include: Warnscale Bottom in the Lake District, Yosemite Valley, and the Rottal and Engstlige valleys in Switzerland. Geologists did not always believe that glaciers were responsible for U-shaped valleys and other glacial erosional features. Ice is quite soft and it was unbelievable to many

neg: Dylife Gorge Way (Welsh: "Llwybr Glyndŵr") passes nearby. Dylife Gorge The Dylife Gorge, located near Dylife, Powys, Mid Wales, was carved by the action (and aftermath) of the last Ice age. It is headed by the Ffrwd Fawr Waterfall. Before the last Ice age, the River Twymyn did not flow through the valley. When the valley was filled by a glacier, the ice ground out a U-shaped glaciated valley. When the glacier that filled the valley melted the Twymyn started to run down the wide channel left behind and the fast flowing river further eroded the valley, cutting the V-shaped gorge as

neg: Dylife Gorge Dylife Gorge The Dylife Gorge, located near Dylife, Powys, Mid Wales, was carved by the action (and aftermath) of the last Ice age. It is headed by the Ffrwd Fawr Waterfall. Before the last Ice age, the River Twymyn did not flow through the valley. When the valley was filled by a glacier, the ice ground out a U-shaped glaciated valley. When the glacier that filled the valley melted the Twymyn started to run down the wide channel left behind and the fast flowing river further eroded the valley, cutting the V-shaped gorge as seen today. The long-distance footpath Glyndŵr's

neg: Napeequa River the Napeequa but was captured by the Chiwawa. The Napeequa Valley has been compared to the fabled Shangri-La. The valley is part of the Glacier Peak Wilderness. Fred Beckey calls the Napeequa River valley the "most interesting valley" of the region. It is a classical glacier-carved U-shaped trough, flat bottomed and nearly straight. Its present form was created by a Pleistocene era glacier. The lower valley is so broad and flat the Napeequa River meanders slowly through it. Near Twin Lakes the Napeequa makes an abrupt westward turn, leaving its valley through a steep gorge cut through the gneiss rock

neg: Side valley can be seen in higher mountain ranges - e.g. in the "young" Rocky Mountains, in the "old" ranges and fjords of Scandinavia, or in the Eastern Alps (Salzach or Inn valley). Whereas the valleys near the "river flats" don't have special forms, the shape of "alpine" valleys depends much more from the former glaciology and of the rock type. Like the main valleys described above, the side- or secondary valley can be V-shaped or U-shaped. Also the valley floor varies - from just a few meters up to some 100 m (e.g. Bad Gastein or St. Moritz, where small towns

neg: Mount Timpanogos Ice Age glaciers mantled the peak until relatively recently, and dramatically shaped the mountain into an Alpine tableau of knife-edge ridges and yawning, U-shaped amphitheaters. A remnant of these glaciers persists in the deeply recessed hanging valley below the main summit. Timpanogos Glacier is a rock-covered mass found on a long, north-facing slope, and usually has patches of snow the entire year. Although an above ground cirque glacier was present before the Dust Bowl Drought of the 1930s, no glacial ice is visible today. However, in 1994, a large crevasse opened up, revealing that there still is a glacier buried

neg: Croagh Patrick Croagh Patrick Croagh Patrick (), nicknamed the Reek, is a mountain and an important site of pilgrimage in County Mayo, Ireland. It is from Westport, above the villages of Murrisk and Lecanvey. It is the third highest mountain in County Mayo after Mweelrea and Nephin. It is climbed by pilgrims on Reek Sunday every year, which is the last Sunday in July. It forms the southern part of a U-shaped valley created by a glacier flowing into Clew Bay in the last Ice Age. Croagh Patrick is part of a longer east-west ridge; the westernmost peak is called Ben Gorm.

neg: U-shaped valley will spread out evenly in open areas, but tend to carve deep into the ground when confined to a valley. Ice thickness is a major contributing factor to valley depth and carving rates. As a glacier moves downhill through a valley, usually with a stream running through it, the shape of the valley is transformed. As the ice melts and retreats, the valley is left with very steep sides and a wide, flat floor. This parabolic shape is caused by glacial erosion striving to decrease friction as much as possible. There are two main variations of this U-shape. The first

neg: Erosion beneath the ice is created. Though the glacier continues to incise vertically, the shape of the channel beneath the ice eventually remain constant, reaching a U-shaped parabolic steady-state shape as we now see in glaciated valleys. Scientists also provide a numerical estimate of the time required for the ultimate formation of a steady-shaped U-shaped valley - approximately 100,000 years. In a weak bedrock (containing material more erodible than the surrounding rocks) erosion pattern, on the contrary, the amount of over deepening is limited because ice velocities and erosion rates are reduced. Glaciers can also cause pieces of bedrock to crack

neg: Cyclopean stairs change in the bedrock type. The stronger bedrock will remain in the form of a riser at the end of a hanging valley. Cyclopean stairs can also form at points where tributary glaciers feed into larger central glaciers. The tributary glacier causes the central glacier to thicken and downcut more rapidly. This may cause a very sudden drop in the valley floor at the points where the glaciers converged. They may also form at the head of a glacier. In an area where the snowline is rising, the cirque in which the glacier forms my recede. A new cirque may

neg: Horseshoe Park It was removed the land was the property was returned to its natural habitat. From 1933 to 1942, the Civilian Conservation Corps operated a camp in Horseshoe Park, and the men removed beetle-infested trees, built and improved trails and campgrounds, and other projects. The park is in the lower elevations of Rocky Mountain National Park, within in the montane ecosystem of forests and grasslands. The U-shaped valley was formed by the movement of a 500-foot thick glacier over hundreds of years. About 15,000 years ago, the glacier pushed through the valley, receded, was deposited rubble into a terminal down the

neg: Mount Shasta of deep glacial erosion except, paradoxically, for its south side where Sargents Ridge runs parallel to the U-shaped Avalanche Gulch. This is the largest glacial valley on the volcano, although it does not now have a glacier in it. There are seven named glaciers on Mount Shasta, with the four largest (Whitney, Bolam, Hotlum, and Wintun) radiating down from high on the main summit cone to below primarily on the north and east sides. The Whitney Glacier is the longest, and the Hotlum is the most voluminous glacier in the state of California. Three of the smaller named glaciers occupy

neg: Queets River of Mount Olympus, and Queets Glacier, on the north side of Mount Queets. The river flows through a narrow canyon, cascading over Service Falls en route, to a point just below Paull Creek, where the valley opens up a bit. From there the river flows generally west to just below Kilkelly Creek, then south to just below Alta Creek, where the valley width expands once more into a typical U-shaped valley glacial river valley. The Queets then flows generally southwest, collecting numerous tributaries including the Clearwater River, Salmon River, and Sams River before emptying into the Pacific Ocean near the

neg: Fjord Fjord Geologically, a fjord or fiord (, ) is a long, narrow inlet with steep sides or cliffs, created by a glacier. There are many fjords on the coasts of Alaska, Antarctica, British Columbia, Chile, Greenland, the Faroe Islands, Iceland, Kamchatka, the Kerguelen Islands, New Zealand, Norway, Novaya Zemlya, Labrador, Nunavut, Newfoundland, Quebec, Scotland, South Georgia Island, and Washington state. Norway's coastline is estimated at with nearly 1,200 fjords, but only when fjords are excluded. A true fjord is formed when a glacier cuts a U-shaped valley by ice segregation and abrasion of the surrounding bedrock. According to the standard

neg: Buried valley glacier itself. Buried valleys are traditionally V- or U-shaped due to the natural shape of valleys, but buried valleys can exhibit different shapes if there were any sort of erosional events after the glacier had finished retreating. The ability to hold groundwater comes from the makeup of the glacial outwash deposits. The glacial outwash deposits of these preexisting valleys mainly consist of coarser materials, such as sand and gravel. Since these materials are coarser, when there is a soil that is almost purely made of these materials, the pore space of the soil increases. This increased pore space creates more

neg: Geology of Monmouthshire west of the county having taken place on one or more occasions. The Vale of Ewyas in the Black Mountains and the Sirhowy Valley, Rhymney Valley, Ebbw Vale and the valley of the Ebbw Fach in the Coalfield bear the hallmarks of glacial excavation - U-shaped profiles and over-steepened sides. There are moreover stretches of glacial till spread across their flanks. Substantial moraines are evident in the Usk valley including the Nevill Hall/Llanfoist moraine south of Abergavenny and the Usk Moraine which is believed to represent the furthest advance of an Usk valley glacier during the last Ice Age. The

neg: Fjord model, glaciers formed in pre-glacial valleys with a gently sloping valley floor. The work of the glacier then left an overdeepened U-shaped valley that ends abruptly at a valley or trough end. Such valleys are fjords when flooded by the ocean. Thresholds above sea level create freshwater lakes. Glacial melting is accompanied by the rebounding of Earth's crust as the ice load and eroded sediment is removed (also called isostasy or glacial rebound). In some cases this rebound is faster than sea level rise. Most fjords are deeper than the adjacent sea; Sognefjord, Norway, reaches as much as below sea

neg: Geology of New England composed of alternating layers of sand and gravel that have been deposited in deltas of glacial lakes and alluvial fans. The slow and grinding movement of continental ice sheets and alpine glaciers across the landscape creates erosional landforms. Abrasion, plucking, and freeze-thaw action creates the U-shaped valley unique to glacial erosion. The intense pressure from the ice causes abrasion. This process carves striations, or grooves, into the bedrock as the glacier moves down a slope. Glacial striations help determine the direction of a glacier; visible outcrops in the White Mountains, for instance, indicate ice flow toward the south-southeast. Abrasion also

neg: Brain terrain indicate the ridges are 4-5 meters high. Brain terrain has been observed to form from what has been called an "Upper Plains Unit." The process begins with the formation of stress cracks. The upper plains unit fell from the sky as snow and as ice coated dust. Today it is widely accepted that glacier-like forms, lobate debris aprons, lineated valley fill, and concentric fill are all related in that they have the same surface texture. Glacier-like forms in valleys and cirque-like alcoves may coalesce with others to produce lobate debris aprons. When opposing lobate debris aprons converge, linear valley fill

neg: River Pushpawati River Pushpawati River Pushpawati flows through the Valley of Flowers in Chamoli district in Garhwal region of the Indian state of Uttarakhand. The Pushpawati rises from the East Kamet Glacier, near Rataban, at the base of the Himalayas near the central part of the Garhwal-Tibet border. It flows in a southerly direction to join the Bhyundar Ganga near Ghagharia. The combined stream is thereafter known as the Lakshman Ganga. The latter merges with the Alaknanda River at Govindghat. The Puspawati drains the Valley of Flowers. The glaciated upper valley of the Pushawati is U-shaped. The river flows past thick glacial

neg: Yihun Lhatso Yihun Lhatso Yihun Lhatso (), also transliterated from Tibetan as Yilung Latsho, is a glacial lake in the Tibetan area of western Sichuan Province, China. Yihun Lhatso rests in a valley on the north side of the Chola Mountains at the foot of Rongme Ngatra. It is found 10km south of the town of Manigango in Dege County, Garze Prefecture. The lake occupies a u-shaped valley and is contained by the former terminal moraine of a glacier originating from Rongme Ngatra that has now receded to above sea level. The lake is drained by the Tro Chu (), a tributary

neg: Paternoster lake in a row; Lake Shelbourne, Swiftcurrent Lake, Lake Josephine, Grinnel lake, and Upper Grinnel Lake all form a nice "rosary" that has produced some spectacular photographs. The U shape of the valley confirms that it was formed by a glacier long ago, as opposed to a V shaped valley cut by a river. More good examples of paternoster lakes can be found in Waterton Lakes National Park, Canada. The three Carthew lakes are in a hanging cirque, reflecting their glacial origins, with Anderson Lake lower in elevation but still clearly part of this paternoster lake procession. Another good example can

neg: Garibaldi Volcanic Belt by the Helmet Glacier. It consists of volcanic ash, lapilli and dispersed ropy and lava bomb segments that bring the cone's prominence to . Its minimal degree of erosion indicates that it might have erupted in the past 1,000 years. A series of basaltic andesite flows were erupted from Cinder Cone about 11,000 years ago that traveled into a deep north trending U-shaped valley on the eastern flank of The Black Tusk. Subsequent volcanism produced another sequence of basaltic lava flows 4,000 years ago that flowed in the same glacial valley. The Black Tusk, a black pinnacle of volcanic rock

neg: Fitzsimmons Creek Fitzsimmons Creek Fitzsimmons Creek is a large creek in Whistler, British Columbia, Canada, having its origins at the Fitzsimmons Glacier in the Garibaldi Ranges of the Coast Mountains. For half its length of approximately 10 kilometres, the creek courses a U-shaped glacial valley which separates two ski mountains of the Whistler Blackcomb resort, Blackcomb to the north and Whistler to the south. Issuing onto the relative lowland of the Whistler Valley just adjacent to Whistler Village, the creek turns more northwest, flowing past the White Gold residential area and entering Green Lake just east of Mons. Fitzsimmons Creek is a

neg: Lake Wanaka but the peaks are somewhat lower. Wanaka lies in a u-shaped valley formed by glacial erosion during the last ice age, more than 10,000 years ago. It is fed by the Matukituki and Makarora Rivers, and is the source of the Clutha River. Nearby Lake Hāwea lies in a parallel valley carved by a neighbouring glacier eight kilometres to the east. At their closest point (a rocky ridge called The Neck), the lakes are only 1,000 metres apart. Small islands towards the foot of the lake include Ruby Island, Stevensons Island and Harwich Island. Some host ecological sanctuaries, such as

neg: June Lake, California Lake's looped valley, often described as a horseshoe-shaped canyon, was formed by glacial action. The Rush Creek glacier split in two when it encountered the resistant rock of what is now known as Reversed Peak. The main glacier flowed toward the north creating the Rush Creek Canyon. Another glacial branch turned south and east but its flow was impeded and eventually stopped as the granitic bedrock on this southern branch created an uphill path toward the volcanic area of the Mono Craters. When the glacier receded it left behind terminal moraine material in the area now known as Oh! Ridge.

neg: Cirque glacier Cirque glacier A "cirque glacier" is formed in a cirque, a bowl-shaped depression on the side of or near mountains. Snow and ice accumulation in corries often occurs as the result of avalanching from higher surrounding slopes. If a cirque glacier advances far enough, it may become a valley glacier. Additionally, if a valley glacier retreats enough that it is within the cirque, it becomes a cirque glacier again. In these depressions, snow persists through summer months, and becomes glacier ice. Snow may be situated on the leeward slope of a mountain, where it is sheltered from wind. Rock fall

neg: Gap of Dunloe last ice age as a result of a "glacial breach" where a glacier in the "Black Valley", part of the Templenoe Icecap, estimated to be over 500 metres deep, broke through the "Head of the Gap" and moved northwards carving out a U-shaped valley. The pass runs north-south between the Old Red Sandstone mountain ranges of the MacGillycuddy's Reeks (to the west) and the Purple Mountain Group (to the east). The north-south road through The Gap as the area is also known, goes from "Kate Kearney's Cottage" in the north, to the highest point at the "Head of the Gap"

neg: Miller Creek (Sixtymile River) it widens and shows a tendency to assume a more curved, or U-shaped, outline in cross-section, thus suggesting a glacial amphitheater or cirque. It is indeed probably to ice action that this broadening and flattening is due. In the winter ice and snow accumulate and have a tendency to move from the dividing ridge down the steep slopes which the rapidly cutting stream has left. During the spring months, when the ice is softening and melting, the head of the valley is occupied by a veritable though small and transient glacier. The rounding of the head of the valley and

neg: Sultan River intense glaciation during the Pleistocene era. The river flows through a well-defined glacially carved trench. The upper South Fork Sultan River flows through a classic U-shaped valley cut by a glacier through Quartz diorite. The Sultan's river main tributaries—the North Fork, South Fork, Elk Creek, and Williamson Creek— flow through narrow valleys to converge in the lower Sultan basin where the valley floor is relatively broad. The Sultan River exits this basin by plunging abruptly into and through a narrow canyon. Pleistocene glaciers spread down the valleys of the Sultan River and its tributaries, merging in the lower basin. From

neg: Rongbuk Glacier Rongbuk Glacier The Rongbuk Glacier () is located in the Himalaya of southern Tibet. Two large tributary glaciers, the East Rongbuk Glacier and the West Rongbuk Glacier, flow into the main Rongbuk Glacier. It flows north and forms the Rongbuk Valley north of Mount Everest. The famous Rongbuk Monastery is located at the northern end of the Rongbuk valley. Mount Everest is the source of the Rongbuk Glacier and East Rongbuk Glacier. The English climber George Mallory first explored the main Rongbuk Valley and its glacier while searching for possible routes to the summit of Mount Everest during the first

neg: Oil lamp was round with nozzles of different forms (volute, semi-volute, U shaped), with a closed body and with a central disk decorated with reliefs and its filling hole. The High Imperial Type. More decorations. Produced locally or imported in large scale. The multiple-nozzled lamps appear. Different varieties. In this period we find the frog type lamps. These are kidney or heart shaped or oval. With the motif of a frog or its abstraction, and sometimes with geometrical motifs. They were produced around 100 AD. They are so variant that it is seldom that two identical ones are found. Slipper shaped. Very

neg: Kings River (California) glaciated during successive ice ages, with valley glaciers flowing as much as down the river's three forks, carving the "V"-shaped river canyons into the "U"-shaped gorges of Kings Canyon, Tehipite Valley and others. The Sierra is composed mainly of granitic igneous rock; however, in the foothill area the Kings River flows through roof pendant formations of older sedimentary and metamorphic rock which were accreted to the Sierra Nevada crustal block as it rose above the surrounding landscape. The lower Kings River forms a large and gently sloping inland delta, or alluvial fan, extending laterally across the Central Valley – the

neg: Reintal (Wetterstein) the west and the Schachen in the east. The lower Reintal lies in the area of the former glacial lake of the Loisach Glacier, into which the Reintal Glacier flowed from the southwest. It is a V-shaped valley and has been predominantly shaped by the Partnach river. Together with the Höllental valley to the north, the Reintal divides the Wetterstein Mountains into several ridges. The northern periphery is formed by the arêtes of the Höllentalspitzen (2,743 m) and the "Hohe Gaifkopf" (1,864 m). The highest points on the southern flank of the valley lie on the Hochwanner (2,744 m), the

neg: Glacier Creek (Turnagain Arm) cut a steep, narrow, V-shaped valley in the mountains west of Glacier Creek, which it joins from the arm. Its bedrock comprises the same materials found on Crow Creek. The gravels are similar, also, but carry less granite and do not show in the same degree the effect of glacial action. Winner Creek joins Glacier Creek just below the mouth of Crow Creek. Its valley, bedrock, and gravels resemble those of California Creek. Glacier Creek (Turnagain Arm) Glacier Creek is a stream flowing out of the Chugach Mountains, which enters the Turnagain Arm of Cook Inlet near Girdwood, Alaska. Crow

neg: Seitz Canyon The canyon then drops to the north as a spectacular headwall of over to a nearly level basin that includes Seitz Lake. It is here that the greatest evidence for glacial sculpturing can be found. The canyon shows a classic U-shaped cross section, and many patches of bare granite still retain the dark patina and striations caused by direct contact with the lower surface of the glacier that once filled this valley. From Seitz Lake the canyon makes a more gradual descent to its middle section , an area that includes a dense stand of aspen trees and beaver ponds.

neg: Fjord led to excavation of the deepest fjord basins. Near the very coast the typical West Norwegian glacier spread out (presumably through sounds and low valleys) and lost their concentration and reduced the glaciers' power to erode leaving bedrock thresholds. Bolstadfjorden is deep with a treshold of only , while the deep Sognefjorden has a threshold around deep. Hardangerfjord is made up of several basins separated by thresholds: The deepest basin Samlafjorden between Jonaneset (Jondal) og Ålvik with a distinct treshold at Vikingneset in Kvam. Hanging valleys are common along glaciated fjords and U-shaped valleys. A hanging valley is a tributary

neg: Hoh River on the north. The former settlement of Oil City is located on the north side of the Hoh River about a half mile from its mouth. A large headland peninsula called Hoh Head is located on the Pacific coast a few miles north of the river's mouth. The South Fork Hoh River originates at , flowing from Hubert Glacier and other small glaciers on the south side of Mount Olympus. It flows generally west through Olympic National Park collecting many tributary streams. At about river mile 11 it enters a broad glacially carved U-shaped valley and becomes braided. The South

neg: Overdeepening glaciers constrained by mountainous terrain as well as tunnel valleys formed on the periphery to the continental glaciers which characterize ice ages. Fjords are formed when a glacier cuts a U-shaped valley by erosion of the surrounding bedrock. Most fjords are overdeepened (i.e., deeper than the adjacent sea). Fjords generally have a sill or rise at their mouth caused by reduced erosion toward the mouth and added to by the previous glacier's terminal moraine, in some cases causing extreme tidal currents with accompanying saltwater rapids. The Sognefjord in Norway stretches inland. It reaches a maximum depth of below sea level,

neg: Coledale (Cumbria) Coledale (Cumbria) Coledale is a valley in the northwestern region of the Lake District in Cumbria, England. Coledale is a narrow U-shaped valley running approximately north-east towards the Derwent Valley floodplain and the village of Braithwaite at the northeastern end. The valley river Coledale Beck feeds into Newlands Beck and is fed by small streams from the valley sides and head, including Birkthwaite Beck, and Pudding Force. At the head of the valley a large rock formation is found named Force Crag, which forms a waterfall 'Low Force' as Pudding Beck passes over it. The valley is ringed by peaks

neg: Palatinate Forest Wikipedia article. Characteristic of the Lower and Middle Bunter are V-shaped valleys, with narrow floors and steep sides, cutting deeply into the bedrock. They are the typiscal valley forms in the central Palatinate Forest, whilst in the southern and northern parts, U-shaped valleys with wider floors predominate. In the southwestern part of the Forest are the so-called "woog" valleys, in which the valley floor is wide and they are therefore especially well suited for the construction of ponds, or "woogs", reservoirs and small lakes (see below). A typical feature of the Palatinate Forest is its abundance of water, that has

neg: Turnagain Arm is the tallest mountain rising from the north side of Turnagain. Mountains rise precipitously on both sides of the arm and reach altitudes of . Their tops are ragged and bare. The timber rarely reaches higher than feet. The smaller valleys are narrow and steep, but the larger ones frequently show by their U-shaped cross section the former presence of glaciers. Glaciers may be still seen at a number of places. Chief among them are Portage Glacier, occupying the Portage Valley between the head of Turnagain Arm and Passage Canal, the two neighboring glaciers which form the headwaters of the

neg: Valley the Scandinavian ice sheet during the various ice ages advanced slightly uphill against the lie of the land. As a result, its meltwaters flowed parallel to the ice margin to reach the North Sea basin, forming huge, flat valleys known as "Urstromtäler". Unlike the other forms of glacial valley, these were formed by glacial meltwaters. Depending on the topography, the rock types and the climate, a lot of transitional forms between V-, U- and plain valleys exist. Their bottoms can be broad or narrow, but characteristic is also the type of valley shoulder. The broader a mountain valley, the lower

neg: Rongbuk Glacier Asia Society and MediaStorm, Breashears' GlacierWorks has made the photos available online. In 80 years, the Rongbuk has shrunk by more than 300 vertical feet across the entire glacier, approximately the height of the Statue of Liberty. Rongbuk Glacier The Rongbuk Glacier () is located in the Himalaya of southern Tibet. Two large tributary glaciers, the East Rongbuk Glacier and the West Rongbuk Glacier, flow into the main Rongbuk Glacier. It flows north and forms the Rongbuk Valley north of Mount Everest. The famous Rongbuk Monastery is located at the northern end of the Rongbuk valley. Mount Everest is the

neg: U-shaped valley anywhere from ten to hundreds of meters deep. These then fill in with sediments to create plains or water to create lakes, sometimes referred to as "string-of-pearl" or ribbon lakes. Such water filled U-valley basins are also known as "fjord-lakes" or "valley-lakes" (Norwegian: "fjordsjø" or "dalsjø"). Gjende and Bandak lakes in Norway are examples of fjord-lakes. Some of these fjord-lakes are very deep for instance Mjøsa (453 meters) and Hornindalsvatnet (514 m). The longitudinal profile of a U-shaped, glaciated valley is often stepwise where flat basins are interrupted by thresholds. Rivers often dig a V-shaped valley or gorge through the

neg: Moraine they reside between and are composed of unconsolidated debris deposited by the glacier. They are created during temporary halts in a glacier's retreat. A medial moraine is a ridge of moraine that runs down the center of a valley floor. It forms when two glaciers meet and the debris on the edges of the adjacent valley sides join and are carried on top of the enlarged glacier. As the glacier melts or retreats, the debris is deposited and a ridge down the middle of the valley floor is created. The Kaskawulsh Glacier in the Kluane National Park, Yukon, has a

neg: Rampsgill Head Rampsgill Head Rampsgill Head is a fell in the English Lake District, standing to the west of Haweswater Reservoir in the Far Eastern Fells. It forms the focal point of three ridges which fan out north-east, north-west and south. The spine of the Far Eastern Fells, travelling north from High Street, crosses the Straits of Riggindale and then collides head-on with the steep U-shaped valley of Rampsgill which comes south to meet it. The ridge splits in two, sending one arm around each side of Rampsgill and the Martindale valley system of which this forms part. The north-western branch leads

neg: Mountains of East Kerry m. Despite most of the area consisting of a bog-covered plateau, some dramatic features created by the last ice age can be seen: Glenacappul, or the Horse's Glen, is a deep U-shaped valley just to the east of Mangerton; the Devil's Punchbowl is a corrie lake below Mangerton's summit to the west; and Lough Guitane is a large lake created when meltwater filled a depression in the ground created by a glacier. Mountains of East Kerry The Mountains of East Kerry, also called the Mangerton Mountains, are a range of mountains situated immediately to the south and east of Killarney

neg: High Desert Discovery Scenic Byway National Register of Historic Places. There is also a modern visitor center located at the barn site. The Steens Loop Tour Route begins at Frenchglen. It is a loop that climbs to the top of Steens Mountain and then descends, re-connects with the main byway south of Frenchglen. From the "East Rim Overlook", travelers can see the Alvord Desert below. The route passes "Kiger Gorge Overlook", a viewpoint above a deep U-shaped glacier cut valley. The route passes several other viewpoints along the crest of Steen Mountain as well. The tour provides an opportunity to spot Bighorn sheep on the

neg: Banff National Park east and over top younger rocks during the Laramide orogeny. Mountain building in Banff National Park ended approximately 55 m.y.a. The Canadian Rockies may have towered up to approximately 70 m.y.a. Once mountain formation ceased, erosion from water and greatly augmented later from glacier ice beginning with the Quaternary glaciation 2.5 m.y.a. carved the mountains into their present shapes. Glacial landforms dominate Banff's geomorphology, with examples of all classic glacial forms, including cirques, arêtes, hanging valleys, moraines, and U-shaped valleys. The pre-existing structure left over from mountain-building strongly guided glacial erosion: mountains in Banff include complex, irregular, anticlinal, synclinal, castellate,

neg: Little Cottonwood Canyon peak was named after Chuck Pfeiffer, a Wasatch Club leader from long ago. Little Cottonwood Canyon Little Cottonwood Canyon lies within the Wasatch-Cache National Forest along the eastern side of the Salt Lake Valley, roughly 15 miles from Salt Lake City, Utah. The canyon is part of Granite, a CDP and "Community Council" designated by Salt Lake County. The canyon is a glacial trough ("U" shaped canyon), carved by an alpine glacier during the last ice age, 15,000 to 25,000 years ago. A number of rare and endemic plant species are found in the canyon's Albion Basin. Mountain goats inhabit

neg: Somesville, Maine see today was largely formed around 380 million years ago by the collision of the continent and an arc of islands, which created the granites and other igneous rocks that comprise most of the island and its mountains. This is how the mountainous landscape came into being. As recently as one million years ago, a mile-thick glacier moved a few yards each year and eventually reached the Mount Desert Range. During this glacial event, Somes Sound was carved out of the island, giving it a curved "U"-shaped valley characteristic of glaciation. Today, many types of rock are on the island,

neg: Little Cottonwood Canyon Little Cottonwood Canyon Little Cottonwood Canyon lies within the Wasatch-Cache National Forest along the eastern side of the Salt Lake Valley, roughly 15 miles from Salt Lake City, Utah. The canyon is part of Granite, a CDP and "Community Council" designated by Salt Lake County. The canyon is a glacial trough ("U" shaped canyon), carved by an alpine glacier during the last ice age, 15,000 to 25,000 years ago. A number of rare and endemic plant species are found in the canyon's Albion Basin. Mountain goats inhabit the surrounding mountains. The Salt Lake Temple of the LDS Church was built

neg: Coniston Water Coniston Water is an example of a ribbon lake formed by glaciation. The lake sits in a deep U-shaped glaciated valley scoured by a glacier in the surrounding volcanic and limestone rocks during the last ice age. To the north-west of the lake rises the Old Man of Coniston, the highest fell in the Coniston Fells group. " 'The king's estate or village'. The 2nd el.[ement] is OE tūn, and the whole name may, like numerous English Kingstons, be from OE 'cyninges-tūn'. ... Scand[inavian] influence is, meanwhile, shown by the '-o-' of early and modern spellings, and Ekwall speculated that

neg: Grand Teton National Park the mountains. The peaks themselves were carved into horns and arêtes and the canyons were transformed from water-eroded V-shapes to glacier-carved U-shaped valleys. Approximately a dozen glaciers currently exist in the park, but they are not ancient as they were all reestablished sometime between 1400 and 1850 AD during the Little Ice Age. Of these more recent glaciers, the largest is Teton Glacier, which sits below the northeast face of Grand Teton. Teton Glacier is long and wide, and nearly surrounded by the tallest summits in the range. Teton Glacier is also the best studied glacier in the range, and

neg: Cathedral Group the remaining dozen glaciers in the Teton Range are located in this cluster of high peaks, including the Teton Glacier which is the largest one in the range. Other glaciers such as the Middle Teton Glacier, Teepe Glacier, and Schoolroom Glacier are also located here. The Cathedral Group has several high cirques, arêtes as well as hanging and U-shaped valleys which are all the work of glacial activity. At the base of the Cathedral Group, several glacial lakes can be found, including Jenny, Bradley and Taggart Lakes, all of which were formed when the glaciers of the last ice age

neg: Selside Pike was raised in the 1940s to provide drinking water supplies. The eastern side of the fell forms the head of Swindale proper, the upper valley being known as Mosedale. Swindale is a classic U-shaped valley, its profile almost a square section, with a flat base and sheer walls. Selside Pike's eastern slopes fall gently to about the 2,000 ft contour and then plunge over a wall of crag to the valley floor. Geordie Greathead Crag is the dominant feature and below this is the dry tarnbed of Dodd Bottom. Hobgrumble Gill falls down this face in a deep gully, separating

neg: Dlaboka River the Ribnička river. The upper course of the river flows through a typical glacial U-shaped valley. The valley narrows at the lower part and forms a canyon. Dlaboka River Dlaboka River (, "Dlaboka Reka"; ), literally meaning "Deep River", is a river in western Macedonia located in the Upper Reka region. It is a left tributary to Ribnička river, which is one of the largest tributaries of Radika river. Its source is high on Mount Korab, forming a steep valley which is one of the few places with alpine climate in Macedonia. The famous Korab waterfall is located near the

neg: Zugspitze wind gap ("Riffelscharte", ). From here the ridge of the "Waxensteinkamm" stretches away over the Riffelspitzen to the Waxenstein. The "Platt" or "Zugspitzplatt" is a plateau below the summit of the Zugspitze to the south and southeast which lies at a height of between . It forms the head of the Reintal valley and has been shaped by a combination of weathering, karstification and glaciation. The area contains roches moutonnées, dolines and limestone pavements as a consequence of the ice ages. In addition moraines have been left behind by various glacial periods. The "Platt" was completely covered by a glacier

neg: Arête ridgeline rather than ascending the headwall either of that glacier or (on the other side of the cleaver) of Emmons Glacier. Notable examples of arêtes include: Arête An arête is a narrow ridge of rock which separates two valleys. It is typically formed when two glaciers erode parallel U-shaped valleys. Arêtes can also form when two glacial cirques erode headwards towards one another, although frequently this results in a saddle-shaped pass, called a col. The edge is then sharpened by freeze-thaw weathering, and the slope on either side of the arete steepened through mass wasting events and the erosion of

neg: Kalabaland Glacier Glacier are Bamba Dhura 6,334 m, Chiring We 6,559 m, Suli Top 6,300 m, Trigal 5,983 m, Burphu Dhura 6,144 m, Suitilla 6,373 m and Kalabaland Dhura 6,105 m. Kalabaland Glacier is nestled by the horseshoe-shaped Himalayan massif separating Goriganga and Lassar Yankti valleys, and it lies a little to the east of the Milam Glacier. The Ralam Gad River originates from the Kalabaland, Yangchar and Sankalp glaciers. Kalabaland Glacier Kalabaland Glacier of Himalaya is situated in the eastern Kumaun of the Pithoragarh district of Uttarakhand state of India. Kalabaland is situated to the north of the Milam Valley and

neg: Stanislaus River occurred during glacial and interglacial periods in the Pleistocene, starting about 1 million years ago. During the ice ages California had a much wetter climate; average river flows in the past may have been as high as what is considered "flood stage" today. The climate was also cold enough to support large glaciers in the Sierra Nevada at elevations above . These glaciers carved large U-shaped valleys in the high elevations, and supplied vast volumes of meltwater which accelerated erosion along the foothill canyons of the Stanislaus River. During the last glacial period the main Stanislaus glacier was up to

neg: Terra Sabaea by the glacier. The center is hollowed out because the ice is mostly gone. These supposed alpine glaciers have been called glacier-like forms (GLF) or glacier-like flows (GLF). Glacier-like forms are a later and maybe more accurate term because we cannot be sure the structure is currently moving. Another, more general term sometimes seen in the literature is viscous flow features (VFF). A variety of other features on the surface have also been interpreted as directly linked to flowing ice, such as fretted terrain, lineated valley fill, concentric crater fill, and arcuate ridges. A variety of surface textures seen in

neg: Doda River Doda River The Doda River or the Stod River is a river long, which forms the Stod Valley in the Zanskar valley of the Ladakh region in the Indian state of Jammu and Kashmir. The Doda River rises from the Drang-Drung Glacier near Pensi La, a mountain pass off the Zanskar-Kargil road. The Drang-Drung Glacier is a river of ice and snow by itself and is the largest glacier other than the Siachen Glacier in Ladakh outside the Karakoram Range. It gives rise to a mountain peak named "Doda Peak", high, and it is the namesake for the Doda district,

neg: Wrangell–St. Elias National Park and Preserve shaped by the competing forces of volcanism and glaciation. Mount Wrangell is an active volcano, one of several volcanoes in the western Wrangell Mountains. In the St. Elias Range, Mount Churchill has erupted explosively within the past 2,000 years. The park's glacial features include Malaspina Glacier, the largest piedmont glacier in North America, Hubbard Glacier, the longest tidewater glacier in Alaska, and Nabesna Glacier, the world's longest valley glacier. The Bagley Icefield covers much of the park's interior, which includes 60% of the permanently ice-covered terrain in Alaska. At the center of the park, the boomtown of Kennecott exploited one

neg: Taylor Glacier Taylor Glacier The Taylor Glacier is an Antarctic glacier about long, flowing from the plateau of Victoria Land into the western end of Taylor Valley, north of the Kukri Hills, south of the Asgard Range. The middle part of the glacier is bounded on the north by the Inland Forts and on the south by Beacon Valley. The glacier was discovered by the British National Antarctic Expedition (1901–04) and at that time thought to be a part of Ferrar Glacier. The Western Journey Party of the British Antarctic Expedition 1910 determined that the upper and lower portions of what was

neg: Mission Mountains have extended 4,000 feet above the valley floor. The glacier reached hundreds of miles down the Rocky Mountain Trench, ending as far south as St. Ignatius, Montana. At the northern end of the range, the glacier flow split, part flowing slowly into the Swan Valley. A view of the area at that time would have been majestic, with large glaciers flowing around both sides and partially over the range. Smaller glaciers would have also flowed out of the mountains and joined the larger one in the valley. This explains the southward pointed hook-shaped ridges at the end of each canyon

neg: Plucking (glaciation) Plucking (glaciation) Plucking, also referred to as quarrying, is a glacial phenomenon that is responsible for the erosion and transportation of individual pieces of bedrock, especially large "joint blocks". This occurs in a type of glacier called a "valley glacier". As a glacier moves down a valley, friction causes the basal ice of the glacier to melt and infiltrate joints (cracks) in the bedrock. The freezing and thawing action of the ice enlarges, widens, or causes further cracks in the bedrock as it changes volume across the ice/water phase transition (a form of hydraulic wedging), gradually loosening the rock between

neg: Christian IV Glacier Christian IV Glacier Christian IV Glacier ( or "Kong Christian den IV's Gletscher") is a large glacier on the east coast of the Greenland ice sheet. It is named after King Christian IV of Denmark (1577 – 1648). Administratively this glacier is part of the Sermersooq Municipality. The area surrounding Christian IV Glacier is uninhabited. The Christian IV Glacier is a non-surge type valley glacier that does not drain the ice sheet directly, but flows partly from it across the mountainous areas of the Gronau Nunataks through the Gronau Glacier and the Grønlands Styrelse Glacier tributaries. Further south it separates

neg: Aviator Glacier the water for about . The name was recommended by the Advisory Committee on Antarctic Names (US-ACAN) in association with Aviator Glacier. Aviator Glacier Aviator Glacier is major valley glacier in Antarctica that is over long and wide, descending generally southward from the plateau of Victoria Land along the west side of Mountaineer Range, and entering Lady Newnes Bay between Cape Sibbald and Hayes Head where it forms the Aviator Glacier Tongue. A glacier is a mass of ice with sufficient thickness to flow away from the source area in lobes, tongues or masses. Glaciers are usually found at high

neg: Aviator Glacier Aviator Glacier Aviator Glacier is major valley glacier in Antarctica that is over long and wide, descending generally southward from the plateau of Victoria Land along the west side of Mountaineer Range, and entering Lady Newnes Bay between Cape Sibbald and Hayes Head where it forms the Aviator Glacier Tongue. A glacier is a mass of ice with sufficient thickness to flow away from the source area in lobes, tongues or masses. Glaciers are usually found at high altitudes or high elevations. The glacier was photographed from the air by Captain W.M. Hawkes, US Navy, on the historic first flight

neg: Mendoza River Mendoza River The Mendoza River is a river in the province of Mendoza, Argentina. It is formed in the Andes range between the Aconcagua and the Tupungato, by the confluence of the Vacas, the Cuevas and the Tupungato rivers, the last being its major tributary. The upper valley of the Mendoza begins at around above mean sea level, and it is U-shaped, of glacial origin. The river reaches Uspallata, then crosses the Precordillera through the Potrerillos Valley, flows along the Cacheuta Canyon and reaches the plain. It forms an arc and turns northeast, finally emptying into the Bañados de Guanacache,

neg: Orjen m, over to the interior. At the main summit of Orjen and the surrounding ridges and high plateaus the action of quaternary glaciation is evident. During the Ice Age, long valley glaciers receded from Orjen to the Bay of Kotor and surrounding poljes. Hollowing U-shaped valleys and cirques in their course. Glaciers also shaped jagged peaks and ridges. Glacial and karst type relief combine now in a unique coastal scenery. There are few places elsewhere in the Mediterranean which demonstrate similar phenomena. The Natural and Culturo-Historical Region of Kotor is a UNESCO World Heritage site, comprising the territory between Orjen

neg: HiWish program images that have been released from the HiWish program as of March 2016. Some landscapes look just like glaciers moving out of mountain valleys on Earth. Some have a hollowed-out appearance, looking like a glacier after almost all the ice has disappeared. What is left are the moraines—the dirt and debris carried by the glacier. The center is hollowed out because the ice is mostly gone. These supposed alpine glaciers have been called glacier-like forms (GLF) or glacier-like flows (GLF). Glacier-like forms are a later and maybe more accurate term because we cannot be sure the structure is currently moving.

neg: Mariner Glacier on the mainland. Named by NZGSAE, 1958–59, as a tribute to the work of mariners in Antarctic research and exploration. Mariner Glacier Mariner Glacier is a major glacier over long, descending southeast from the plateau of Victoria Land, between Mountaineer Range and Malta Plateau, and terminating at Lady Newnes Bay, Ross Sea, where it forms the floating Mariner Glacier Tongue. Its lower reaches and entrance to its valley were reconnoitered in December 1958 by Captain John Cadwalader, US Navy, and two members of New Zealand Geological Survey Antarctic Expedition (NZGSAE), in a flight from the icebreakers USS "Glacier" and USS

neg: Valley recedes or thaws, the valley remains, often littered with small boulders that were transported within the ice. Floor gradient does not affect the valley's shape, it is the glacier's size that does. Continuously flowing glaciers – especially in the ice age – and large-sized glaciers carve wide, deep incised valleys, sometimes with valley steps that reflect differing erosion rates. Examples of U-shaped valleys are found in every mountainous region that has experienced glaciation, usually during the Pleistocene ice ages. Most present U-shaped valleys started as V-shaped before glaciation. The glaciers carved it out wider and deeper, simultaneously changing the shape.

neg: Mariner Glacier Mariner Glacier Mariner Glacier is a major glacier over long, descending southeast from the plateau of Victoria Land, between Mountaineer Range and Malta Plateau, and terminating at Lady Newnes Bay, Ross Sea, where it forms the floating Mariner Glacier Tongue. Its lower reaches and entrance to its valley were reconnoitered in December 1958 by Captain John Cadwalader, US Navy, and two members of New Zealand Geological Survey Antarctic Expedition (NZGSAE), in a flight from the icebreakers USS "Glacier" and USS "Staten Island" which were lying close off the south end of Coulman Island, in an attempt to land expedition members

neg: Blatten (Lötschen) hotel. The Jungfrau-Aletsch protected area, includes most of the municipality, although excluding the main settlements. At the head of the Lötschental valley, the Lötschenlücke pass, into the valley of the Aletsch Glacier, forms the municipal boundary. Below this pass, the Langgletscher glacier occupies the Lötschental valley, whilst the Schwarzsee lake lies at a lower level. The valley is framed by the Tschingelhorn to the north and the Bietschhorn to the south, and the slopes of both mountains lie within the municipality. Blatten has an area, , of . Of this area, 9.5% is used for agricultural purposes, while 9.0% is

neg: Mendenhall Valley, Juneau at the intersection of Glacier Highway and Mendenhall Loop Road at Auke Bay. The Valley comprises an area stretching from the wetlands along Fritz Cove and Auke Bay back to the Mendenhall Glacier as well as Mendenhall Lake and the Mendenhall River, which for the most part drains the Valley. The Valley forms the core of Alaska's 34th election (or state House) district, which is represented in the Alaska House of Representatives by Justin Redbeard Parish, a Democrat. Along with the rest of Juneau and adjoining communities, it is part of Senate District Q, represented in the Alaska Senate by

neg: Braldu River second highest mountain peak of the world. The Biafo Glacier holds the Snow Lake, which is 61 mile (100 km) river of ice, it is among the world's longest continuous glacier systems outside of the polar regions. The Braldu River flows almost eastwards, entirely in the Skardu District of Baltistan and forms the Braldu Valley. The most remote settlement in the valley is the village of Askole, situated at the right bank of the Braldu River. Askole serves as the base camp for mountaineering expeditions and trekking to the various glaciers in this Karakoram Range. Many glacier fed streams joins

neg: Beta distribution 1906 monograph "Frequency curves and correlation" further analyzes the beta distribution as Pearson's Type I distribution, including a full discussion of the method of moments for the four parameter case, and diagrams of (what Elderton describes as) U-shaped, J-shaped, twisted J-shaped, "cocked-hat" shapes, horizontal and angled straight-line cases. Elderton wrote "I am chiefly indebted to Professor Pearson, but the indebtedness is of a kind for which it is impossible to offer formal thanks." Elderton in his 1906 monograph provides an impressive amount of information on the beta distribution, including equations for the origin of the distribution chosen to be the

neg: Sound (geography) formation. Sometimes a sound is produced by a glacier carving out a valley on a coast then receding, or the sea invading a glacier valley. The glacier produces a sound that often has steep, near vertical sides that extend deep under water. The sea floor is often flat and deeper at the landward end than the seaward end, due to glacial moraine deposits. This type of sound is more properly termed a "fjord" (or "fiord"). The sounds in Fiordland, New Zealand, have been formed this way. A sound generally connotes a protected anchorage. They can be part of most large

neg: Saltfjellet from the coast to the Swedish border. The glacier Svartisen is actually two glaciers, separated by the Glomdalen valley with the Glomåga river. Western Svartisen is the second largest glacier on the Norwegian mainland, and is part of the Saltfjellet-Svartisen National Park. There are many other glaciers as well. A total of of the area is protected. Several long valleys radiate from the mountains, such as the Dunderland Valley and Blakkådalen going south from the mountains, and Saltdal and the Beiar Valley going northwards. The eastern part of the range forms a plateau with some gently sloping mountains, and this

neg: Kolahoi Peak Kolahoi Peak Kolahoi Peak is a mountain with a peak elevation of , in Anantnag district of Jammu and Kashmir, in the vicinity of Sonamarg. Kolahoi Peak is part of the Himalaya Range, and is located between 15 km south of Sonamarg and 21 km north from Arin Pahalgam. To its north flows the Sind River and the glacier of its name Kolahoi Glacier is the source of Lidder River. in the vicinity of Kashmir valley. Kolahoi Peak rises from the Kolahoi Glacier is a pyramid-shaped peak with ice falls and ice fields at its bottom. The rock formation of

neg: Machoi Peak Machoi Peak Machoi Peak is a mountain with a peak elevation of , in Ganderbal district of Jammu and Kashmir, in the vicinity of Sonamarg. Machoi Peak is part of the Himalaya Range, and is located between Amarnath cave and Zojila. It lies 105 km north east from Srinagar, 25 km from Sonamarg in the east. It rises from the glacier of its name Machoi Glacier is the source of Nallah Sindh. in the vicinity of Kashmir valley. Machoi Peak rises from the Machoi glacier is a pyramid-shaped peak with ice falls and ice fields at its bottom and ridges.

neg: Viedma Glacier become entwined within the center of the new glacial ice mass as it forms. At right angles to the glacial moraines in the middle, crevasses, large, canyon-sized cracks, are apparent in the grey-brown ice that can be seen along the sides of the glacier. These cracks are formed from the stress arising between ice along the valley walls (that is slower moving as the friction is greater) and the relatively fast moving ice at the glacier's center. On the southwestern side of the glacier terminus, calving of ice is visible. The glacier terminus ends in a cliff. Viedma Glacier Viedma

neg: Outwash fan Outwash fan An outwash fan is a fan-shaped body of sediments deposited by braided streams from a melting glacier. Sediment locked within the ice of the glacier, gets transported by the streams of meltwater, and deposits on the outwash plain, at the terminus of the glacier. The outwash, the sediment transported and deposited by the meltwater and that makes up the fan, is usually poorly sorted due to the short distance traveled before being deposited. Outwash fans typically form from valley Glaciers in the mountains, that are flowing downhill. Thus, outwash fans are usually found in colder environments where glaciers

neg: Flowers Hills Flowers Hills The Flowers Hills () are a triangular shaped group of hills, long and wide, with peaks of (Gubesh Peak) and (Dickey Peak), extending along the eastern edge of the Sentinel Range, Ellsworth Mountains, Antarctica. The hills are bounded by Hansen Glacier and Dater Glacier to the west and north, Rutford Ice Stream to the east and Sikera Valley to the southwest, and separated from Doyran Heights to the west-southwest by Kostinbrod Pass. Their interior is drained by Lardeya Ice Piedmont and Valoga Glacier. The hills were first mapped by the United States Geological Survey from surveys and U.S.

neg: Places of interest in the Death Valley area is on is part of the Black Mountains which along with the parallel Panamint Range across the valley from what geologists call a horst and the valley that is called a graben. These structures are created when the surface of the earth is under extensional, or a pulling force. The crust responds to this force by sending a large and long roughly v-shaped block of crust down which forms the bedrock of the valley floor (see Basin and Range). Darwin Falls is a waterfall located on the western edge of Death Valley National Park near the settlement of Panamint Springs,

neg: Hadley Upland Hadley Upland Hadley Upland () is a triangular shaped remnant plateau with an undulating surface, , in southern Graham Land, Antarctica. It is bounded by Windy Valley and Martin Glacier, Gibbs Glacier and Lammers Glacier. The existence of this upland was known to the United States Antarctic Service, 1939–41, Finn Ronne and Carl R. Eklund having travelled along Lammers and Gibbs Glaciers in January 1941. The upland was surveyed by the Falkland Islands Dependencies Survey in 1948–50 and 1958, and was named by the UK Antarctic Place-Names Committee after John Hadley, an English mathematician who, at the same time as

neg: Geology of the Death Valley area under playa sediments before they can grow too large. Slot canyons are often found at the mouths of the streams that feed the fans, and the slot canyons in turn are topped by V-shaped gorges. This forms what looks like a wineglass shape to some people, thus giving them their names, "wineglass canyons". This table of formations exposed in the Death Valley area lists and describes the exposed formations of the Death Valley National Park and the surrounding area. Geology of the Death Valley area The exposed geology of the Death Valley area presents a diverse and complex set of

neg: Glacier Blanc form a common system. The Glacier Blanc is a typical valley glacier, which initially runs in a curve towards the northeast below the Barre, before its tongue turns southeast, becoming an icefall. Its average incline is about 30%, but it is flatter in its central section than on the north slope of the Barre des Écrins or in the icefall of its lower section. The glacier is bounded on its orographically left-hand side by, "inter alia", the summits of the Roche Faurio (), Pic de Neige Cordier () and the Montagne des Agneaux (). The "Crête de l'Encoula" forms the

neg: Glacial series "Zungenbecken", the terminal moraines and the gravel plains in front of them. The bowl-shaped basins, which were formed by the scouring of the ground by the glacier, were called "Zungenbecken" ("tongue basins"), because the tongue or snout of the glacier was once located here. In these basins, if there was no outlet, glacial lakes ("Gletscherrandseen" or "Zungenbeckenstauseen") were formed during the retreat of the glacier. There is a number of lakes of this type in the Salzkammergut, for example. Typical landforms within the "Zungenbecken" of the Alpine Foreland are drumlins, but there are rarely any tunnel valleys. Around the "