In the Schöningen open lignite mine (Northeastern Lower Saxony, Germany), Tertiary strata are unconformably overlain by Quaternary sediments and soils of Middle and Late Pleistocene and Holocene age. The complex Pleistocene sequence contains a number of interglacial and interstadial deposits and soils and is of significance for the subdivision of the younger Middle Pleistocene in NW Europe and for archaeological evidence of early human occupation by Homo erectus. Recent studies reveal evidence for three interglacial periods between the Elsterian and the Saalian ice advances. At the base of Holsteinian interglacial deposits, artifacts and remains of large mammals have been excavated. Burnt flint of a fireplace gave a Thermoluminescence age of 450+/-40 ka (D. Richter, unpublished) and suggests a correlation of the Elsterian glacial period with isotope stage 12.

The next youngest warm stage after the Holsteinian, named the Reinsdorf interglacial, is the subject of debate as it has no clear palynostratigraphic equivalent elsewhere in Europe. Recently, layers of travertine of the Homo erectus site of Bilzingsleben (Thuringia, Germany) have been correlated with the Reinsdorf interglacial by palynological data. In addition to pollen, the deposits of the Reinsdorf are also rich in small and large mammal remains, and contain a variety of invertebrates and plant macrofossils. The interglacial layers and soils contain two lower Palaeolithic horizons. Of great importance are seven already excavated, extremely well preserved wooden artifacts (spears) made from spruce trunks, found within the layers of Reinsdorf Interstadial II, following the Reinsdorf interglacial (H. Thieme). These layers are rich in skeletal and bone remains of horses. The spear finds and remains of hunt prey are demonstrating the capability of organized hunting by Early Humans.

The peaty horizon of the Schöningen interglacial is considered to be the youngest of the three interglacial periods. Based on Uranium/Thorium dating of peat, the Holsteinian, Reinsdorf and Schöningen interglacials are tentatively correlated with oxygen isotope stages 11 (Holsteinian > 350 ka), 9 (Reinsdorf about 320 ka) and 7 (Schöningen about 200 ka).

There is evidence of a soil complex developed in glacial sediments of the Drenthe Stadial (Saalian). These Stagno-(Calcaric) Gleysols are overlain by reworked loess-like material with cryoturbations and eolian loess attributed to the Warthe Stadial (Saalian). The hydromorphic duplex soils have not yet been studied in detail.

Travertine and peat layers of the last interglacial (Eemian) were deposited during the second half of the warm stage over a time span of about 6000 years. Local hydrologic conditions during late Eemian interglacial and early glacial (Weichselian) periods have been reconstructed by pollen analysis and plant macro remains, specifically by moss analyses. Eemian peaty layers reveal a Thorium/Uranium age of 115-149 ka (H.Heijnis) and are correlated with oxygen isotope stage 5.

In relation to overall patterns and time correlations of palaeosol sequences, interglacials are regularly and immediately followed by development of heathland, steppe and two or more short forest periods at the transition to a cold period. Interstadials, depending on geographic location, indicate different climatic conditions and are best understood by comparison with the climax vegetation and soil of the preceding interglacial. Therefore, it seems clear that for pedocomplexes of the Mid-Late Quaternary, at least in Central Europe, the first most strongly developed soil of the pedocomplex represents the climax soil of the interglacial. Interstadials, which had temperate forests that follow an interglacial, seem to be related to conditions existing in the respective interglacial isotope stage.