Kames are irregular hills, mounds, terraces or short ridges composed mainly of sand and gravel deposited by meltwater in association with stagnant or decaying glacial ice. They are characteristic of deglaciation landscapes where blocks or masses of glacier ice became isolated from active ice flow and sediment accumulated in depressions, channels or cavities adjacent to or within the stagnant ice. When the buried or surrounding ice eventually melts, the sediment is left as an irregular positive landform or terrace.
Kames are therefore generally depositional features and are commonly associated with complex glaciofluvial environments. Their shapes can vary substantially because their formation depends on the geometry of meltwater channels, ice margins, sediment supply and the arrangement of stagnant ice. Unlike eskers, which commonly form elongated sinuous ridges associated with confined meltwater channels, kames are often more irregular and localised. They can occur together with kettles, kame terraces, eskers and outwash deposits in landscapes affected by stagnant ice decay.
Kame formation is strongly associated with stagnant ice, meaning glacier ice that has become separated from the main actively flowing ice mass and is no longer transported effectively downstream. Meltwater streams can carry sand and gravel across or around the stagnant ice and deposit sediment in channels, hollows or ponds. Sediment may accumulate against an ice margin, within a crevasse, on top of ice or in a depression partly surrounded by ice.
When the ice melts, the supporting geometry disappears and the sediment collapses or remains as an irregular mound depending on how it was deposited. This process explains why kames can have steep or uneven sides and why their surfaces may contain complex internal structures. The presence of stagnant ice is important because the final landform can record the position and geometry of temporary ice bodies rather than simply reflecting the regional topography.
Kame terraces are a particularly recognisable form of Kame. They develop when meltwater streams flow between a glacier margin and the adjacent valley side, depositing sediment in a relatively level terrace. If the glacier later retreats and the ice melts, the former meltwater deposit may remain as a bench or terrace along the valley side. Kame terraces can therefore preserve evidence of former glacier margin positions and meltwater levels.
Their elevation and continuity can help reconstruct the relative position of ice during deglaciation, although interpretation requires consideration of post depositional erosion and deformation. Kame terraces are often composed of stratified sand and gravel, reflecting deposition by flowing water. Their relationship to valley walls, former ice margins and associated glaciofluvial deposits can distinguish them from ordinary river terraces. The presence of buried or melting ice during deposition can also produce irregularities that are not typical of normal fluvial terraces.
Kames commonly contain sorted and stratified sediment because meltwater is responsible for much of their deposition. Sand and gravel can be arranged in layers reflecting changing water discharge, channel position and sediment supply. However, the internal structure of a kame can be highly variable because deposition may occur in several interconnected environments. Some deposits may be laid down by streams, while others accumulate in temporary lakes or ice bounded depressions.
Collapse after ice melting can deform originally horizontal beds, producing tilted, faulted or irregular strata. This makes kames useful records of the complexity of glacial retreat. Sedimentological analysis can identify depositional environments, while geophysical surveys can reveal buried ice or internal structures where they remain preserved. Kames therefore provide evidence not only of glaciofluvial deposition but also of the changing geometry of stagnant ice during deglaciation.
Kames are closely associated with kettles, although the two are different landforms. A kame is primarily a positive depositional feature, while a kettle is a depression formed when a buried or isolated block of glacial ice melts after being surrounded by sediment. Kame and kettle topography can therefore occur together in landscapes affected by stagnant ice. Eskers are also associated with meltwater but tend to form more continuous sinuous ridges representing confined channels.
Moraines are generally composed of sediment deposited directly by glacier ice and commonly have different sedimentological characteristics. Outwash plains are broader surfaces formed by meltwater beyond the ice margin, whereas kames are more localised and often closely associated with stagnant ice. These distinctions are useful because glacial landscapes can contain many sedimentary landforms whose materials may appear superficially similar but whose depositional environments differ.
Kames occur widely in areas formerly covered by Pleistocene glaciers and ice sheets, including Britain, Ireland, Scandinavia, Canada and the northern United States. In Britain, kame landscapes are especially associated with areas where complex glacial retreat produced stagnant ice and abundant meltwater. Kames can influence modern drainage and land use because their permeable sand and gravel may differ sharply from surrounding finer sediments or bedrock.
They can form elevated, relatively well drained sites that have sometimes been used for agriculture, transport or settlement. Their sand and gravel may also be economically valuable, although extraction can alter groundwater systems and geomorphological features. From a scientific perspective, kames are valuable because their distribution can reveal zones of stagnant ice and phases of deglaciation. Their irregular geometry often indicates that ice retreat was spatially complex rather than a simple uniform withdrawal of a coherent glacier front.
The identification of Kames requires attention to geomorphological context because hills and mounds of sand and gravel can form through many non glacial processes. A kame is more convincingly identified when it occurs within a former glacial landscape and shows evidence of meltwater deposition, stagnant ice influence or association with other glaciofluvial features. Modern river deposits can form terraces and bars that may superficially resemble kame deposits, but their relationship to active or former river channels differs.
Landslides can also create irregular mounds but generally contain poorly sorted material and display different structural characteristics. Field investigations can examine sediment sorting, bedding, clast characteristics and relationships to nearby glacial landforms. Digital elevation data can reveal patterns of kame and kettle topography that indicate stagnant ice decay. Reliable interpretation therefore combines morphology, sedimentology, stratigraphy and regional glacial history.
Kames provide important evidence for reconstructing the final stages of glacial retreat. Their formation commonly indicates that ice became stagnant or fragmented while meltwater continued to transport and deposit sediment. This can reveal a transition from actively flowing ice to complex dead ice landscapes. Kame deposits may preserve temporary meltwater channels, ponds and ice margin positions, while associated kettles record locations of buried ice that later melted.
Together these features can demonstrate that deglaciation occurred through a combination of frontal retreat, stagnation, meltwater reorganisation and ice block melting. Their practical and scientific value therefore extends beyond their individual appearance. Kames help explain the three dimensional architecture of glacial sediments and the dynamic processes operating during deglaciation, while their permeable deposits can influence groundwater, soil development, vegetation and human land use long after the original glacier has disappeared.
