Drumlins are streamlined, elongated hills composed of glacial till, with a steep stoss side (up-glacier side) and a gently sloping lee side (down-glacier side). They are significant in interpreting glacial environments as they indicate the direction of glacier movement. Drumlins form beneath a glacier as it reshapes and redeploys the subglacial till. Their aligned, teardrop shape points in the direction the glacier was moving. By studying drumlins, geographers can determine the flow patterns of past glaciers, providing insights into the dynamics of ice movement and the characteristics of the subglacial environment.

Fjords are long, narrow, deep inlets of the sea, flanked by steep cliffs or mountains, created by the deep glacial erosion of valley floors. Their formation begins with a glacier moving down a valley to the sea. As the glacier erodes the valley through plucking and abrasion, it carves a deep U-shaped valley. When the glacier retreats and melts, sea water floods the valley, forming a fjord. The depth and steep sides of fjords are evidence of the glacier's erosive strength. Studying fjords helps in understanding the extent and power of ice age glaciers and the subsequent rise in sea levels that flooded these valleys.

Eskers are long, winding ridges of sand and gravel that form within glacial landscapes. They are created by streams that flow underneath, within, or on top of glaciers. These streams carry sediment that is deposited along their course. When the glacier melts, the stream’s course becomes a ridge, marking where the stream once flowed. Eskers can be several kilometers long and vary in height and width. They are important in understanding the subglacial hydrology of glaciers, revealing the routes of meltwater channels and providing evidence about the nature of the glacier's retreat, such as whether it was steady or punctuated by pauses. Eskers also serve as indicators of the direction of glacial movement.

Hanging valleys are a striking feature in glaciated landscapes, often seen as elevated secondary valleys that join a primary, deeper glacial valley. They form when a smaller tributary glacier flows into a larger main glacier. The main glacier, being deeper and more powerful, erodes the valley floor more vigorously, creating a deeper U-shaped valley. Meanwhile, the tributary glacier, with less erosive power, creates a shallower valley. When the glaciers retreat, the tributary valley is left hanging high above the main valley floor, often leading to the creation of spectacular waterfalls. Hanging valleys are important indicators of the relative size and erosive power of past glaciers, highlighting the dynamics of glacial erosion.

The freeze-thaw cycle is a significant factor in glacial erosion, particularly in the process of plucking. It occurs when water seeps into cracks in the bedrock beneath or at the edges of a glacier. As temperatures drop, the water freezes and expands, exerting pressure on the surrounding rock. This expansion widens the cracks and loosens fragments of the rock. When temperatures rise, the ice melts, allowing the glacier to move. The glacier can then pluck these loosened rock pieces and carry them along. This process is particularly effective in areas with frequent temperature fluctuations around the freezing point, leading to repeated cycles of freezing and thawing, thereby intensifying the erosive power of the glacier.