The lithostratigraphic classification of the Quaternary deposits is based on the genesis of the sediments. The distinguished environments are marine - estuarine, fluvial, eolian and slope. The marine - estuarine deposits are restricted to certain time-intervals within the Quaternary and are limited to the northern part of Belgium. Fluvial deposits are found throughout the Quaternary. On the basis of the sedimentological - lithological differentials within the Meuse basin and the Schelde basin a bipartite subdivision of the fluvial deposits is introduced. Eolian deposits are differentiated on the basis of their grain size distribution, namely sand and silt. The sandy deposits are accumulated in the northern part of Belgium, whereas loess is deposited in the more southern part of the country. Slope deposits are not restricted regionally neither temporally.

Re-alignment of the road near the Rakaia Gorge bridge (S82) has clearly exposed deposits of the Woodlands and younger glacial advances, and their erosional or faulted relationships. Renewed geomorphological mapping in the area indicates that the Tui Creek Advance was in three phases, not one as previously recognised, so that it may have the status of a full glaciation. New details of the deposits and geomorphology related to the three phases of the last ( Acheron) advance of the Otira Glaciation indicate greater aggradation than previously supposed, and the formation of a complex of lakes during fluctuations of the glacier.

Analysis of LiDAR-derived imagery led to the discovery of more than 330 pre-Holocene to recent landslides in Southern Flanders (4850 km2). The morphology of three landslides, including the 266.5 ha deep-seated gravitational slope deformation in Alden Biesen, was investigated in more detail. The analysis of the morphological and topographical characteristics (width–length relation, frequency–area distribution and topographical threshold) of the landslides revealed important differences compared to the characteristics reported in other landslide studies, and helped understanding possible landslide triggering mechanisms. Especially the possibility of a seismic origin of the landslides was investigated. Finally, a heuristic model for region-wide landslide susceptibility mapping was successfully tested. The susceptibility model and map allow prediction of future landslide locations and contribute to better understanding the role of individual causal factors on landslide location and spatial density. The results suggest that landslides on low-gradient, soil-mantled hills are a more important contributor to landscape evolution of hilly areas than was hitherto thought. The morphology of all hilly regions of Flanders is clearly marked by landslide processes and higher landslide densities often coincide with the presence of quaternary active faults. This study further shows that high-resolution topographical data such as LiDAR significantly contributes to a better detection of old, previously unknown landslides.

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Beerse-Dam is localised in the sandy region of Northern Belgium. The sandy and loamy sediments covering the Kempen Clay are of Weichsehan age. The importance of the exposure can be summarized as : 1) Beerse-Dam permitted to show that the ice wedges belonging to a fossil permafrost, are often overlain by an intensily convoluted horizon, representing the active layer. 2) The important cold period characterized by the development of a continuous permafrost at the beginning of the plemglacial, follows an interstadial (probably the equivalent of Odderade) during wich a boreal pine forest covered the Kempen. 3) The "Brabantse leem" in the Kempen can be considered as the equivalent of the Hesbayen loess. It covers a peat dated at 42 000 B P and in it's top a humic soil has developed. With a C14 age of 38 000 B.P this soil coincides with the Hengelo-interstadial. 4) The Wildert coversands rest upon a humic loam. Its position above an important erosion level, its homogeneity and its pollen content in which Pinus in absolutely dominant, resemble the characteristics of Kesselt A at the base of the Brabantien.