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The Geology of the Belvédère Pit and Its Wider Geographical Setting

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The Geology of the Belvédère Pit and Its Wider Geographical Setting The geology of the Belvédère pit and its wider geographical setting 2.1 Introduction The aim of this chapter is to give a short description of the Middie and Late Pleistocene deposits at Maastricht-Belvé- dère in order to provide the reader with a general geological framework, certain aspects of which will be discussed in greater detail in the rest of this volume. Before we concen- trate our attention on the Belvédère-pit, a description will be given of the general geological setting of the Ouaternary deposits at Belvédère in a summary of the geology of the region, i.e. the southern part of the Dutch province of Limburg (2.2). The paragraphs following this regional setting discuss the lithology and lithostratigraphy of the recorded sections in the pit (2.3.2), the palaeosols present (2.3.3), and the palaeoenvironment during the formation of the deposits (2.3.4). Finally, the relative and absolute dat- ing evidence of the different units is presented in section 2.3.5, while section 2.3.6 gives a first synthesis of the Mid­ die Pleistocene sequence at Belvédère. 2.2 The wider geological setting South Limburg is situated in the transitional fault-block area between the Dutch Central Graben and the Ardennes highlands, as shown in figure 7. The continuation of the Central Graben into Germany is called the Rurtal Graben (fig. 7). In general terms, the Ardennes Massif may be seen as an erosional area, while the Central Graben is a deposi- tional environment. In South Limburg there are a large number of southeast/northwest orientated faults, of which the northernmost Feldbiss fault is the most pronounced. In the south, the Central Graben is bounded by the Feldbiss fault and in the north by the Peelrand fault. These faults developed during the Early Tertiary and have affected the geography of sedimentation and erosion in South Limburg Fig. 7. Structural development of South Limburg (after; Kuyl 1980). ever since. The subsoil deposits of the South Limburg area date from the Carboniferous, Cretaceous and Tertiary periods and are Limburg; more extensive remnants occur in the neigh- overlain by Ouaternary deposits, which consist mainly of bouring Belgian and German uplands. The highest hill in fluviatile sediments and loess. the Netherlands, the Vaalserberg, 321 m above Dutch The present-day landscape of South Limburg was sculp- Ordnance Level (NAP), is a slight elevation in the pe­ tured during the Ouaternary by the Maas and its tributaries. neplain. By the end of the Tertiary a peneplain had formed over the In the Early Ouaternary the Maas took a more northeast- Ardennes and their immediate surroundings. Traces of this erly course than at present (called the East Maas) from a peneplain are still visible in the southeastern part of South point near Liège where it left the Ardennes to join the 10 THE GEOLOGY OF THE BELVÉDÈRE PIT AND ITS WIDER GEOGRAPHICAL SETTING 1 4 5 8 10 11 13 Fig. 8. The Maas terrace geomorphology of South Limburg; drawing based on data provided by the State Geological Survey at Heerlen (pers. comm. PW. Bosch and W.M. Felder, 1980-1985). The numbers refer to the symbols used for the different terrace bodies: 1 =Waubach (Terti- ary deposits), 2=Kosberg, 3=Simpelveld, 4=Margraten, 5=Sibbe, 6=Valkenburg, 7=St.Geertruid, 8=St.Pietersberg, 9='s Gravenvoeren, 10=Rothem, 11 =Caberg, 12=Eisden-Lanklaar, 13=Oost-Maartand. See also Table 2. (The posltion of the Belvédère pit is indicated by an asterisk.) The A-B line refers to the cross-section shown in figure 9. Rhine in the environs of the town of Jülich (West Germa- during the Early Pleistocene and eventually caused the river ny). A wide and shallow valley was formed in the pene- to shift its northeasterly course to a more westerly one, plain, traces of which are still visible in the landscape (Kuyl called the West Maas. After every change of course, the 1980). river cut deeper into the landscape, leaving behind the old During the later Quaternary a series of river terraces was river deposits as elevated terraces. The older the Maas formed along the Maas in South Limburg; the most com­ sediments, the higher they lie south of the Feldbiss fault. plete series is found to the south of the Central Graben. The The terrace system of the Maas, traditionally divided into terrace formation was related to the epirogenetic upheaval Higher, Middle and Lower Terraces with several subdivi- of the southeastern part of South Limburg, which began sions, has been the object of much research (Brueren 1945; 11 THE WIDER GEOLOGICAL SETTING Fig. 9. Cross-section through the terrace landscape of South Limburg, along the A-B line indicated in figure 8. For the symbols used for the terrace bodies see figure 8 (after: Brueren 1945). The position of the Belvédère pit is indicated by an asterisk. Van Straaten 1946; Zonneveld 1955; Paulissen 1973; Dop- sequence south of the Central Graben represents only a few pert et al. 1975; Felder et al. 1980; Kuyl 1980). The nomen- episodes of the total stratigraphical time range of the Qua- clature of the terrace sequence now in use is shown in table ternary (Zagwijn 1985). 2. Figure 8 shows the terrace geomorphology of South In the Central Graben itself sedimentation was more Limburg based on new maps recently provided by the State continuous than in the region south of the Feldbiss, where Geologicai Survey (W.M. Felder and P. Bosch, pers. sedimentation alternated with erosion. In fact, the sedi­ comm., 1980-1985). The new results differ only slightly mentary sequence preserved in the Central Graben provides from the resuhs of Brueren (1945), on which the cross- the most complete sequence of the Dutch Quaternary sections through the terrace landscape shown in figure 9 are known. Quaternary sediments in this region are over 200 m based. thick in places (cf. Zagwijn/De Jong 1983-1984). Evidence concerning the ages of the different terraces is In the later part of the Pleistocene South Limburg was still scarce (table 2). The few biostratigraphical data avail- covered by loess deposits, which today vary in thickness able have been summarized by Zagwijn (1985). Pollen from a few dm to more than 20 m. Figure 10 (after: Kuyl analysis of a sample from a peat bed discovered in the 1980) gives the distribution of loess deposits of over 5 m uppermost part of the Simpelveld Higher Terrace deposits thick in South Limburg. In recent years the loess deposits in suggests a Late Tiglian date for the formation of these this region have been the object of detailed research, using sediments (Platte Bosschen locality). Sediments of the physical and chemical methods developed for the earth Valkenburg Higher Terrace at Süsterseel are overlain by a Sciences, such as thephrostratigraphy, micromorphology loess deposit with reversed magnetic polarity (Van Mont- and thermoluminescence (TL) dating (cf. Juvigné 1977; frans 1971), and pollen analysis of a peat bed found at the Meijs 1980; Kuyl 1980; Vreeken/Mücher 1981; Haesaertset boundary between the terrace gravel and the overlying loess indicates that the peat was formed during the Bavel in- terglacial of the Early Pleistocene and thus has an age of 900 ka (Zagwijn/De Jong 1983-1984). Table 2: The Pleistocene terrace sequence in South Limburg, with indications of the ages of the terraces as discussed in the text. Finally, gravels of the Caberg Middle Terrace deposits at Maastricht-Belvédère are overlain by sediments whose general subdivision name age faunal contents indicate that they were formed in an intra- SaaUan warm-temperate phase (section 8.3 of this volume; Lower Terrace Oost-Maarland see also: Van Kolfschoten/Roebroeks 1985). The gravels Eisden-Lanklaar Late Saalian themselves contain the remains of a cold fauna, which have Caberg Early Saalian been assigned an Early Saalian age (Van Kolfschoten 1985). Middle Terrace Rothem In addition to this biostratigraphical evidence. Bruins s'Gravenvoeren (1980) has found (unpublished) indications of the presence St Pietersberg of the Brunhes-Matuyama boundary in the Sint-Geertruid St Geertruid Brunhes-Matuyama? deposits at Nagelbeek. Paulissen (1973) identified a Middle Higher Terrace Valkenburg Bavel interglacial Terrace younger than the Caberg terrace, but still dating Sibbe from the Saalian, showing that a typical Eemian Interglacial Margraten Simpelveld Late Tiglian soil had developed in the Eisden-Lanklaar terrace deposits. Kosberg The available data suggest that the fluviatile sedimentary 12 THE GEOLOGY OF THE BELVÉDÈRE PIT AND ITS WIDER GEOGRAPHICAL SETTING r ^s .-. _ Vaals Fig. 10. Distribution of loess layers 8 km of over 5 metres thick (1) and the northern boundary of the loess (2) in South Limburg (after: Kuyl 1980). al. 1981; Juvigné/Semmel 1981; Meijs et al. 1983; Mees/ oped during each westward shift and incision phase of the Meijs 1984; Meijs 1985; Vandenberghe et al. 1985; Hux- river, which then formed their own valleys in the terrace table/Aitken 1985; Bouten et al. 1985; Wintle 1987). landscape, each with its own series of side valleys formed by There are three diagnostic horizons in the loess stratig- smaller rivulets. The dry valleys show great variation in size raphy of the region: and morphology. Usually, a dry valley system has a dendrit- - the Sol de Rocourt (Gullentops 1954), interpreted as ical structure, the largest dry valleys connecting up to a (remnants of) a soil of Eemian age, which was formed in valley through which water flows all the year round. Saalian loess; - the Eltville tuff, a thin volcanic ash bed present in the Because of the large number of stream valleys and dry toppart of the WeichseUan 'Middle Silt Loam' (cf.
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