Austria's longest glacier, the Pasterze, winds its 8 km (5 mile) route at the foot of Austria's highest mountain,
A number of geologic features are associated with glaciers, including moraines that form from glacially transported rocks and debris at the terminus of the glacier; distinctive U-shaped valleys[?] (cwms[?]); and cirque valleys[?] at their heads.
The upper part of a glacier that receives most of the snowfall is called the zone of accumulation. The snowfall here is sufficiently heavy to exert a downward force and cause deep erosion of rock in this area, often leaving a bowl or amphitheater-shaped depression called a glacial cirque[?]. On the opposite end of the glacier, at its foot or terminal end, is the zone of deposition (also called the zone of wastage or the zone of ablation) where upward and lateral forces predominate and deposition of sediment occurs. Between these two zones is the line of equilibrium where the downward erosive forces of the zone of accumulation and the upward deposition forces of the zone of deposition cancel. Erosive lateral forces are not canceled; therefore, glaciers turn v-shaped river-carved valleys into u-shaped glacial valleys.
Glacial moraines are formed from the deposition of material from a glacier and are exposed after the glacier has retreated. These features usually appear as linear mounds of till, which is a poorly-sorted mixture of rock, gravel and boulders that are within a matrix of a fine powdery material. Terminal or end moraines are formed at the foot or terminal end of a glacier, lateral moraines are formed on the sides of the glacier, and medial moraines are formed down the center. Less obvious is the ground moraine which often blankets the surface underneath much of the glacier downslope from the line of equilibrium. Other features formed by glacial deposition include distinctive streamlined hills known as drumlins, and long snake-like ridges formed by streambeds under glaciers, known as eskers. Glacial meltwaters contain rock flour[?], an extremely fine powder ground from the underlying rock by the glacier's movement.
So-called "stoss and lee erosional features" are formed by glaciers and show the direction of its movement. Long linear features that follow the direction of movement are called glacial striations[?] and divots in the rock are called chatter marks[?]. These two features are both left on the surfaces of stationary rock that were once under a glacier and were formed when loose rocks and boulders in the ice were transported over the rock surface. Transport of fine-grained material within a glacier can smooth or polish the surface of rocks, leading to what geologists call glacial polish[?]. Glacial erratics[?] are rounded boulders that were left by a melting glacier and are often seen perched precariously on exposed rock faces after glacial retreat.
Some glaciers are quite small, while others may be tens of kilometers in length. Today, they are found on very high mountains in equatorial and mid-latitude regions and progressively lower as one approaches the poles. Greenland and Antarctica are heavily glaciated, to the point of being almost entirely covered by ice. Glaciation of this extent is called continental glaciation.
The downstream end of continental glaciers often flows into the sea. As the ice reaches the ocean, it breaks off, forming icebergs.Glaciers are really rivers of ice that move slowly downhill. Even in very cold climates, there may be unglaciated areas, which receive too little precipitation to form permanent ice.
The snow from which glaciers form is subject to repeated freezing and thawing, permitting the formation of a form of granular ice called nevé. Under the pressure of the layers of ice and snow above it, this granular ice fuses into solid glacial ice. Glacial ice contains minute air bubbles as a result, giving it a distinctive blue tint due to Rayleigh scattering. The lower layers of glacial ice flow and deform plastically under this pressure, allowing the glacier as a whole to move slowly like a viscous fluid. Glaciers do not need a slope to flow, being driven by the continuing accumulation of new snow at their source. The upper layers of glaciers are more brittle, and often form deep cracks known as crevasses[?] as they flex. These crevasses make travel over glaciers a risky proposition. Glacial meltwaters flow throughout and underneath glaciers, carving channels in the ice similar to caves in rock and also helping to lubricate the glacier's movement.
During ice ages, continental glaciers may be as much as 1500 meters thick. A more extreme instance of glacial growth may have occurred during the Snowball Earth period. In the past several centuries the Earth's glaciers have generally been retreating, often dramatically.
See also: West Antarctica[?]