МАКСИМАЛЬНАЯ ГРАНИЦА СКАНДИНАВСКОГО ЛЕДНИКОВОГО ПОКРОВА В ВАЛДАЙСКУЮ (ВИСЛИНСКУЮ) ЭПОХУ И ОСОБЕННОСТИ РЕЛЬЕФА ЕГО ПЕРИФЕРИЧЕСКОЙ ЗОНЫ

Abstract

After the end of the Mikulino interglacial, in connection with the rising cooling trend, the Scandinavian ice sheet began to form on the territory of Fennoscandia. Its development to the maximum boundaries was accompanied by the ice sheet advances and retreats that reflected the succession of colder and warmer climate phases over a long period, called the Valdaian (Weichselian, Vistulian) ice age. The Scandinavian ice sheet did not reach its maximum simultaneously at different lobes. The age of the maximum boundary on becomes younger from west to east, which is associated with the paleoclimatic situation in the North of Eurasia due to the formation of an extra-continental climate. Climate continentality increased eastward along the periphery of the ice sheet. These climate features and the ice sheet response determined the nature of glacial morphogenesis in the proglacial zone. The conditions for the formation of a peripheral ice sheet and an increase in the number of mudflows and the formation of glacial lakes were more favorable during the ice sheet degradation than its expansion. Therefore, the forms of active and dead ice, especially the terminal moraines and kames of different types, the valleys of marginal channels and outwash plains serve as the hallmarks of the stages of warming and degradation of ice sheets.