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Am Tönchesberg und in Koblenz-Metternich sind über dem Bt-Horizont des Eems (OIS 5e) bis an die Basis des Oberweichsel-Löß (OIS 2) zehn eigenständige Bodenbildungen nachgewiesen, die durch Sedimentationsphasen voneinander getrennt sind. Bis auf die beiden jüngsten, die als braune Tundrenböden anzusprechen sind, handelt es sich um gut ausgeprägte Ah-Horizonte, z. T. um Bv-, Bt-Ah- bzw. Bt-Horizonte., research

The River Rhine is one of the few major fluvial systems that connect the areas of the Alpine glaciers and Scandinavian ice sheet and so provides a key for correlating the two glacial areas in northern and middle Europe. The fluvial sequences of the Rhine Valley include at least 11 Pleistocene terraces in the Lower Rhine area, 2 Pliocene and 12 Pleistocene terraces in the Middle Rhine area resulting in 15 different Pliocene and Pleistocene terraces based on the correlation between Lower and Middle Rhine. The formation of fluvial terraces is significantly influenced by climatic and tectonic processes. The terrace staircases are a result of uplift in the Middle Rhine area and the southern part of the Lower Rhine area, whereas subsidence in the northern part of the Lower Rhine area resulted in buried stacked sequences. Magnetostratigraphic data provide chronological constraints for the terrace deposits in the Lower Rhine embayment and Middle Rhine region. The Matuyama/Brunhes boundary is a reliable marker horizon for the Upper Terrace fluvial deposits exposed in the Karlich clay pit in the Middle Rhine area. The first appearance of volcanic heavy mineral grains in the terrace sediments, in loess and soils can be correlated from the Middle Rhine area through the Lower Rhine embayment to the Netherlands. The first occurrence of Nordic components in terrace sediments of the Lower Rhine area is known from gravel on top of the Kempen-Krefeld beds and so are younger than the Holsteinian but older than the penultimate glaciation. In the lower Middle Rhine area, 40Ar/39Ar dating of tephra layers intercalated in the aeolian and fluvial sediments provide age constraints. The Upper Pleistocene aeolian sediments overlying the terrace deposits have been dated by luminescence methods, and the tephra from the Laacher See eruption (12,860 BP) is present in the Younger Lower Terrace deposits.

Loess, loess-like sediments and the intercalated palaeosols along the bluffs of the river Yenisei provide a detailed Upper Pleistocene climate archive for the southern part of Middle Siberia. The section at Kurtak is one of the most detailed loess/palaeosol sequences in Middle Siberia. Two major periods of sediment accumulation were recorded in the sequence: the stratigraphically oldest one post-dating the last interglacial palaeosol and pre-dating the Kurtak Pedocomplex (oxygen isotope stage (OIS) 3); the younger one post-dating the Kurtak Pedocomplex and predating the Holocene soil. Three major phases of soil formation occurred during the Upper Pleistocene. The Kameny Log Pedocomplex (OIS 5e) consists of at least two pedogenetic episodes, a lower clayey chernozem forming during a more humid and warmer climate than today, and an upper chernozem representing a drier climate than today, the latter one including a well-pronounced carbonate-rich horizon. The Sukhoy Log Pedocomplex consists of a chernozem-like palaeosol and two kastanozjems (OIS 5c-a) and the Kurtak pedocomplex (OIS 3) with two chernozem-like palaeosols and up to three humic-rich layers. Additionally, weakly developed gleyed horizons are considered to represent palaeohydrological groundwater high levels. The results indicate a synchronous evolution of climate and environment change in both the more oceanic driven climate of West and Central Europe and Middle Siberia, as evidenced by luminescence dating results.

The loess/palaeosol sequence of Kurtak, situated at the western bank of the upper Yenisei in Middle Siberia, represents one of the best developed Middle and Upper Pleistocene sediment records in Yenisei Siberia. More than 40 m thick loess and loess-like sediments intercalated by at least four pedocomplexes are exposed at a steep erosional slope at the bank of the Krasnoyarsk Water Reservoir. Infrared optically stimulated luminescence (IRSL) and thermoluminescence (TL) dating techniques have been applied on 38 fine grain samples from the upper 23 m of the profile, representing the penultimate and last interglacial–glacial cycle. The IRSL and TL age estimates are in good agreement with the geological estimates up to the last interglacial soil horizon (oxygen isotope substage (OIS) 5e). The luminescence ages show that the lowermost truncated palaeosol of kastanosjem-type is likely to have formed during the penultimate interglacial upon subaerial deposits. Three weak reddish brown palaeosols intercalated by reworked loess-like sediments correlate with early Upper Pleistocene interstadials (OIS5dion of -a), and a succession of humic horizons alternated by cryoturbation processes (Kurtak pedocomplex) is linked with OIS 3. Thick loess deposits between the pedocomplexes show now significant age increase with depth, indicating high accumulation rates at around 23 ka (OIS 2) and 60 ka (OIS 4).

The loess–palaeosol sequences of the Middle Rhine Area provide a relatively detailed and continuous terrestrial record of climate and environment change for the past 200,000 years. Loess–palaeosol sequences are generally well preserved in inter- and intra-crater depressions of late Middle Pleistocene scoria cones in the East Eifel Volcanic Field and on fluvial terraces of the lower middle terrace of the rivers Rhine and Moselle. Stratigraphic and chronological investigations of loess–palaeosol sequences from sections at Tonchesberg and Koblenz–Metternich in the Middle Rhine Area indicate that the last interglacial and glacial cycle is preserved in much more detail than previously thought. In both sections, the last interglacial soil is covered by at least ten palaeosols, postdating the Eemian (oxygen isotope (sub)stage, OIS 5e) brown forest soil.

Das Profil der Tongrube Kärlich wurde geologisch neu bearbeitet, mit folgenden Ergebnissen: 1. Die Einstufung von Abschnitt A in den Jaramillo-Event ist nicht bewiesen. Abschnitt A kann jünger sein und damit in den Bavel-Komplex gehören. 2. Der quartäre Vulkanismus der Osteifel setzt in der Warmzeit ein, die Abschnitt F abschließt. Es gibt Hinweise im Profil von Kärlich, daß in der Westeifel der quartäre Vulkanismus schon deutlich früher, schon in der Matuyama-Epoche, einsetzte. 3. Eine Unterteilung von Abschnitt G, im Sinne von Razi Rad (1976), gibt es nicht und hat es nicht gegeben. Alle Sedimente von Abschnitt G zeigen eine Dominanz von brauner Hornblende im Schwermineralspektrum. 4. Abschnitt H ist durch die markanteste Diskordanz des gesamten Profils in Abschnitt H-unten und Abschnitt H-oben geteilt. 5. Das „Kärlicher Interglazial" ist zu unterteilen in ein Kärlicher Interglazial I, unter dem Brockentuff und ein Kärlicher Interglazial II, über dem Brockentuff. Die beiden Interglaziale sind durch mindestens eine Kaltphase voneinander getrennt., research