In Kola Peninsula, Karelia and Northern Dvina Basin the Late Valdai age of moraines of the last glaciation formed by the ice of the Scandinavian Shield is generally recognized. East of the Kuloi Plateau, down to the Lower Ob River, opinions of different scientists concerning the age of moraines associated with expansion of the Barents, Novaya Zemlya and Kara ice covers, differ. Some of them date these moraines by the Late Valdai; the others assign them to the Early Valdai. In the light of available data the first point of view is more well-grounded. In reference outcrop Vastyanovsky Kon' in the Lower Pechora the Late Valdai moraine, in the structure of which interglacial sediments take part (MIS 3), is characterized in accordance with samples from fossil seed floras by five radiocarbon datings: 24,790 -29,470 (see article by A.V. Goldberg et al. in the collection of papers "Pleistocene of Siberia and adjacent areas" 1973, pp. 151-178). Later radiocarbon dating of the allochtonous peat in interglacial sediments showed the out-of-limit age of the main part of samples (Kh.A. Arslanov et al., 1987), as well as numerous datings on bulk sample and selectively taken plant fragments (J. Mangerud et al., 1999). However, the age of mammoth tusk, extracted from a washout in a sand spit, is in the interval between 32,440±850 and 39,000±850 (A.S. Lavrov, L.M. Potapenko "Neopleistocene of the north-east Russian Plain", 2005, p. 86)

In all areas of the western Russian Arctic, bounded from the south by the Arctic Circle, formations of the Late Valdai glaciation (Ostashkov, Polar, Polar-Urals and Sartansk in accordance with stratigraphic charts in force) are noted for well preserved eskers, kames, moraine relief and numerous lakes. Marginal facies of this glaciation with numerous stadial and oscillation ridges have a complicated structure and a peculiar distribution. For example, in the boundaries of Kola Peninsula (as well as within the limits of Kanin Peninsula, see article by Y.A. Lavrushin and O.G. Epshtein in the Bulletin of the Commission on the Quaternary study, 2001, No 64, pp. 35-60) along with widely developed moraines of Scandinavian origin, stadial formations associated with the thrust of the Barents Sea ice in the second half of MIS 2 are observed.

In the boundaries of Bolshezemelskaya tundra, Pai-Khoi and Western Cisurals ultimate moraines of the Late Valdai show up distinctly in remote images. They clearly enough differ from the Early Valdai moraines (MIS 4).

In the Northern part of the Polar Urals ice covers, which came from the north, caused the valley-meshy character of the Late Valdai glaciation. Not only local, but also transit ice took part in this glaciation. Approximately to the latitude 67°40' in the west and 67°20' in the east this ice prevented local ice from outflowing the foothills area. The most representative and local foothill moraines south of the front of transit moraines are observed in the Bolshaya Usa River valley in the west (N 67°20') and in the Longotien River valley in the east (67° 10'), where they descend to absolute elevations 150-200 m. Marginal facies of the foothill moraine of the Sob glacier (N 67°) occur at the same elevations in the area of Polyarny Ural railway station, where its ultimate ridges are locally inserted into erosional hollows cutting a young (MIS 2-3) foothill valley.

Reference:

Borisov B.A. Age of the last glaciation in the western Russian Arctic. Correlation of Pleistocene Events in the Russian North. International Workshop Abstracts. 4-6 December 2006. Saint-Petersburg, 2006, p. 20.