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Tidewater glaciers are glaciers that terminate in the sea, including most glaciers flowing from Greenland, Antarctica, Baffin, Devon, and Ellesmere Islands in Canada, Southeast Alaska, and the Northern and Southern Patagonian Ice Fields. As the ice reaches the sea, pieces break off or calve, forming icebergs. Most tidewater glaciers calve above sea level, which often results in a tremendous impact as the iceberg strikes the water. Tidewater glaciers undergo centuries-long cycles of advance and retreat that are much less affected by climate change than other glaciers.[17]

Mouth of the Schlatenkees Glacier near Innergschlöß, Austria.
Mouth of the Schlatenkees Glacier near Innergschlöß, Austria.

The Grotta del Gelo is a cave of Etna volcano, the southernmost glacier in Europe.
The Grotta del Gelo is a cave of Etna volcano, the southernmost glacier in Europe.

Sightseeing boat in front of a tidewater glacier, Kenai Fjords National Park, Alaska.
Sightseeing boat in front of a tidewater glacier, Kenai Fjords National Park, Alaska.

Classification by thermal state

Webber Glacier on Grant Land (northern Ellesmere Island) is an advancing polar glacier and frozen to the glacier bed. Debris rich layers of the ground moraine are sheared and folded into the ice. The steep icefront shows waterfalls. The glacier front is 6 km broad and up to 40 m high (July 20, 1978)
Thermally, a temperate glacier is at a melting point throughout the year, from its surface to its base. The ice of a polar glacier is always below the freezing threshold from the surface to its base, although the surface snowpack may experience seasonal melting. A subpolar glacier includes both temperate and polar ice, depending on the depth beneath the surface and position along the length of the glacier. In a similar way, the thermal regime of a glacier is often described by its basal temperature. A cold-based glacier is below freezing at the ice-ground interface and is thus frozen to the underlying substrate. A warm-based glacier is above or at freezing at the interface and is able to slide at this contact.[18] This contrast is thought to a large extent to govern the ability of a glacier to effectively erode its bed, as sliding ice promotes plucking at rock from the surface below.[19] Glaciers which are partly cold-based and partly warm-based are known as polythermal.[18]

Formation
Glaciers form where the accumulation of snow and ice exceeds ablation. A glacier usually originates from a cirque landform (alternatively known as a “corrie” or as a “cwm”) – a typically armchair-shaped geological feature (such as a depression between mountains enclosed by arêtes) – which collects and compresses through gravity the snow that falls into it. This snow accumulates and the weight of the snow falling above compacts it, forming névé (granular snow). Further crushing of the individual snowflakes and squeezing the air from the snow turns it into “glacial ice”. This glacial ice will fill the cirque until it “overflows” through a geological weakness or vacancy, such as a gap between two mountains. When the mass of snow and ice reaches sufficient thickness, it begins to move by a combination of surface slope, gravity, and pressure. On steeper slopes, this can occur with as little as 15 m (50 ft) of snow-ice.

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