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Stratigraphy and sedimentary evolution Westerhoff, W.E.
2009
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citation for published version (APA) Westerhoff, W. E. (2009). Stratigraphy and sedimentary evolution: The lower Rhine-Meuse system during the Late Pliocene and Early Pleistocene (southern North Sea Basin). TNO Built Environment and Geosciences.
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Download date: 28. Sep. 2021 2 A revised lithostratigraphy of Upper Pliocene and Lower Pleistocene fluvial deposits from Rhine, Meuse and Belgian rivers in the Netherlands
W.E. Westerhoff, A. Menkovic & F.D. de Lang
This paper will be published in a special issue of Netherlands Journal of Geosciences on the Upper Tertiary and Quaternary lithostratigraphy of the Netherlands. Scheduled for 2009.
Abstract A thorough revision is presented of the lithostratigraphical units of Upper Pliocene and Lower Pleistocene fluvial deposits in the south- eastern part of the Netherlands. Two new formations are defined: 1 The Waalre Formation includes all mixed Rhine-Meuse deposits. The heavy-mineral composition is characterised by predominantly unstable associations. 2 The Stramproy Formation includes all deposits that are formed by northward flowing rivers that drained the central and northern part of Belgium. The heavy-mineral composition is dominantly stable. Their lower and upper boundaries are formed by regionally extensive and marked stratigraphical horizons like the Reuver Bed at the top North Sea of the Kieseloolite Formation, and the unconformity at the base of the Sterksel Formation. The Waalre Formation is subdivided into three (informal) subunits of which the lower one (WA-1) forms an equivalent of the Late Pliocene Oebel Beds in Germany. The middle subunit (WA-2) mainly occurs in the northern part of the Roer Valley Graben and grades laterally into the shallow marine deposits of the Maassluis Formation. The upper subunit (WA-3) extends over the central and western part of the Netherlands into the present North Sea. Sediments supplied by the Belgian rivers provided infilling of the (remaining) accommodation space in the Roer Valley Graben and Amsterdam adjacent areas after the abandonment of the Rhine-Meuse system from these areas. Both formations occur at least for a part adjacent 3’ Zegveld to each other and show repeated intercalations as a result of the combined effect of tectonic movements and climate change. The revised lithostratigraphic units are defined strictly by lithology and stratigraphic superposition and therefore provide a firm Den Haag framework for the development of 3-dimensional (numerical) geological models and palaeogeographical reconstructions. Utrecht
Rotterdam 2.1 Introduction intermingled with bio- and chronostratigraphic criteria. Peel Boundary fault
Gilze Rijen fault Sedimentary sequences and ages of rocks formed the initial As a result a justified lithostratigraphical assignment often 1’ Northern Roer Valley issues studied by stratigraphers. The evolution of stratigraphy has to be carried out with help of microscopic techniques. Venlo Block has gradually included other aspects such as: morphology, Initially, lithology formed a main criterion to make distinction Graben lithology, fossil content, geophysical and geochemical between rock units. However, the palaeontological subdivision Krefelder Block properties. As a consequence stratigraphy now can comprise of the Pleistocene (Van der Vlerk & Florschütz, 1953; 49G0204 Huijbergen Peel Block all kinds of characteristics and attributes of rocks units. Zagwijn, 1957) and palaeogeographical reconstructions Eindhoven Venlo 3 Rhine However, the core-business of stratigraphy (i.e. the logical (Zonneveld, 1958) determined strongly the concepts of the 51D0343 2’ Tegelen ordering of rock units) still is focused on bio-, chrono-, and geomorphological and depositional architecture (Zagwijn, lithostratigraphy. Lithostratigraphy thereby is seen as the 1963b Roer Valley Graben ). As a consequence the latter aspects provided an 2 Southern basic step in stratigraphic research. It provides a framework increasing influence on the lithostratigraphical classification. 57H0058 1 Köln Feldbiss Faultzone LRE for all kinds of geoscientific studies, especially for geological The intermingling of various criteria eventually has led to Scheldt Kölner Block mapping and subsurface modelling (Weerts & Westerhoff, restricted possibilities for use of the lithostratigraphical 2006). units thus defined in digitally designed numerical subsurface
models that can be used in applied geoscientific research. Jülich Ruhr ScholleErft Block This paper focuses on a pure lithostratigraphical approach Maastricht for the Upper Pliocene1 and Lower Pleistocene fluvial According to the lithostratigraphical scheme of Doppert et Aachen deposits in the southern part of the Netherlands (Fig. 2.1). al. (1975) the Upper Pliocene and Lower Pleistocene fluvial These deposits have been studied already for more than deposits are assigned to three superimposed lithostratigraphic Rhenish Massif Meuse a century (see overview of References by Meijer, 1998). formations (Fig. 2.2). The lowest comprises all Pliocene
Based on their fossil content (small and large mammals, fluvial deposits and was assigned as Kieseloolite Formation. Main depositional direction of Pliocene and Quaternary fluvial systems 0 25 50 km plant macro remains, and pollen) they have played a The middle unit is known as Tegelen Formation, a mixed Major fault Site mentioned in text central role in the establishment of the Quaternary (litho) Rhine-Meuse deposit with an assumed (pre)Tiglian to Early stratigraphic framework of the Netherlands (Zagwijn, 1960, Eburonian age. The third unit is termed the Kedichem Other fault Borehole 51D0343, holostratotype Waalre Fm., a 1963 ; Doppert et al., 1975). However, due to the initial Formation. It overlies the Tegelen Formation and therefore 1 1’ Cross-section see figure 2.4 interest in the palaeontological content of the deposits comprises all fluvial (mixed Rhine-Meuse and Belgian rivers) Belgian rivers Borehole 49G0204, and an overestimated impact of climate change on them, and local deposits that post-date the Tiglian Stage. hypostratotype Waalre Fm., the lithostratigraphic subdivision of the Lower Pleistocene Meuse see figure 2.5 Rhine Borehole 57H0058, fluvial deposits (cf. Doppert et al., 1975) became strongly Figure 2.1. Tectonic setting of the study area and depositional holostratotype Stramproy Fm., direction of main fluvial systems during the Late Pliocene and Eridanos ('eastern' rivers see figure 2.7 originating in the Baltic area) Early Pleistocene. 1 The terms Pliocene and Pleistocene are used here according to the ICS-timetable 2008 where the base of the Pleistocene Series is indicated as identical to the base of the Gelasian Stage at 2.588 Ma (ICS-2008. www.stratigraphy.org).
20 21 behind the two previously defined Tegelen and Kedichem on these marine deposits might probably contribute to a Vlerk & Florschütz, 1953; Pannekoek, 1956). These continental Heavy-mineral Main characteristics Lithostratigraphy Formations have changed considerably and therefore we better understanding of the palaeogeography and ages of the ‘Praetegelen’ deposits were correlated with the marine composition of fluvial deposits cf. Doppert et al., also have replaced the original names of these formations deposits in this part of the Lower Pleistocene sedimentary Amstelian, a stage typified by a mollusc assemblage indicative 1975 (Salvador 1994; Walsh, 2005). Instead, two new formations record. of cool climatic conditions. The overlying marine deposits are introduced: belonged to the Icenian Stage. Tesch made no distinction on Fluvial deposits of Rhine & Sterksel Meuse with Rhine-dominated Formation • the Waalre Formation describes mixed Rhine-Meuse 2.3 Brief review of former stratigraphical approaches the basis of the origin of the fluvial deposits. unstable heavy-mineral association deposits formed during the Late Pliocene and Early The history of Pliocene and Lower Pleistocene stratigraphic Pleistocene. The deposits are dominated by unstable research of the fluvial record in the southern part of the 2.3.2 The sediment-petrographical approach (2) (‘Rhine’) heavy-mineral associations. Netherlands shows four main types of approaches. However, it The stratigraphical approach based on the petrographical Mid Pleistocene Stratigraphy • the Stramproy Formation encompasses deposits that are should be understood that they did not develop independently composition and provenance of sediments (Edelman, 1933, 1938; Baak, 1936) has proven to be a powerful tool for the 3 Fluvial deposits of the Belgian Kedichem mainly formed by rivers draining the central and northern but show close interrelationships. rivers and local material Formation part of Belgium. The heavy-mineral composition comprises characterisation of deposits and mapping of the distributional dominated by stable heavy- a,b mineral associations dominantly a stable assemblage. 2.3.1 The mapping approach (1) areas. Zonneveld (1947 , 1950, 1958) thoroughly elaborated Both new formations occur next to each other and Lorié’s (1907) tripartition of ‘Onderste Grof’ (Lower Coarse), this in his sediment-petrological studies and was able to 2 Fluvial deposits of Rhine & Tegelen interdigitate repeatedly. ‘Middelste Fijn’ (Middle Fine) and ‘Bovenste Grof’ (Upper reconstruct a comprehensive stratigraphy. He also considered Meuse with Rhine-dominated Formation unstable heavy-mineral Coarse) was the first lithostratigraphical classification of the lowermost fluvial sequences typified by a stable heavy- associations 2.2 Depositional setting Pleistocene deposits in The Netherlands (Fig. 3). It was purely mineral content as an equivalent of the German Kieseloolite
Early Pleistocene Tectonically, the south-eastern Netherlands forms part of the based on lithological characteristics. A slightly adapted deposits. Within the Lower Pleistocene fluvial deposits Lower Rhine Embayment (LRE) which is the most south- version was applied by Molengraaff & Waterschoot van Zonneveld distinguished the Zone of Tegelen (unstable heavy- easterly embranchment of the North Sea Basin. The generally de Gracht (1913). As a geological mappper Tesch (1934, mineral associations with a clear presence of garnet) and subsiding LRE is bounded to the south by Palaeozoic rocks 1937) subdivided the deposits according to a mixture of recognised them as Rhine deposits. Based on age correlations of the uplifting Rhenish Massif. The main tectonic features morphostratigraphical, biostratigraphical and lithological Zonneveld considered the terrace deposits of the Meuse 1 Pre-Rhine & Meuse deposits Kieseloolite of this Cenozoic rift system within the Netherlands are the criteria. He correlated the fluvial Pliocene deposits with the in South Limburg as contemporaneous with (but not part with stable heavy-mineral Formation associations subsiding Roer Valley Graben (RVG) situated between the ‘Kieseloolith Stufe’ in the German part of the LRE (Fliegel, of) the Zone of Tegelen. Deposits with a dominant stable Pliocene
Campine Block to the west and the Peel Block to the east 1907; Kaiser, 1907; Tesch, 1908, 1911, 1934; Wunstorf & Fiegel, heavy-mineral assemblage that overlie the sediments of (Geluk et al., 1994). The latter forms part of the so-called 1910) and linked them to the Scaldisian of his mollusc-based, the Zone of Tegelen were first termed the Lower Fine Zone Heavy-minerals Venloër Scholle (Klostermann, 1983). The RVG is confined by marine Pliocene stratigraphy. The Lower Pleistocene fluvial (Zonneveld, 1947b) and subsequently as Serie van Kedichem Unstable minerals Stable minerals major faults systems. The Feldbiss and Gilze Rijen faults form deposits were classified by Tesch as ‘Praeglacial older than (Doppert & Zonneveld, 1955). The typification serie was Garnet Zircon, Rutile a.o. the southern and western border while the Peel Boundary Main Terrace’. The lower part of it was thought to be the chosen because it was expected that ongoing research would fault is the main fault along the east side of the RVG (Fig. 2.1). equivalent of the ‘Praetegelen’ continental deposits (Van der reveal a number of similar zones. Later, Zonneveld (1958) and Epidote Staurolite
Alterite/sauss. Metamorphic m. During the Tertiary Period marine sedimentation dominated in the western part of the LRE while peat was formed in Hornblende Tourmaline extensive swamps in the middle and south-eastern parts. Lorié, 1907 Molengraaff en Tesch, 1934 Zonneveld, 1947 v.d. Vlerk & Doppert & Zonneveld, Induced by uplift of the Rhenish Massif, fluvial deposition Waterschoot Florschütz, 1953 1955 Figure 2.2. Lithostratigraphical concept for Late Pliocene and Early Pleistocene v.d. Gracht, 1913 b began during the Late Miocene. These oldest fluvial sediments fluvial deposits in The Netherlands (according to Zonneveld, 1947 ; Doppert & W S W S Zonneveld, 1955: Zagwijn, 1960, 1963a, Doppert et al., 1975). in the LRE were deposited by a (pre-)Rhine drainage system that did not extend into southern Germany (Boenigk, Upper Coarse Upper Coarse Main Terrace Equivalent of Drenthien Augite Zone of a,b bearing Veghel New mapping results based on a large number of borehole 1978 ; Gliese & Hager, 1978). During the Pliocene, the Meuse (Riss) (Mindel) (Riss) Zone of Zone of (Riss) unit and well-logging data obtained since 1975, have demonstrated established a course through the so-called East Meuse Valley Veghel Veghel (ca. Riss) that the interrelationship of the lithostratigraphical units (Zonneveld, 1974; Kuyl, 1980; Felder & Bosch, 1989; Juvigné (ca. Riss and (ca. Riss) (ca. Riss) younger) discerned is much more complex than hitherto thought. & Renard, 1992; Van den Berg, 1996) in South Limburg and Sediments with a lithological and petrographical composition entered the alluvial plain of the Rhine just north of Jülich. and Serie of Serie of Sterksel RVG younger Sterksel similar to the Tegelen Formation were already deposited Rivers draining the central and northern part of Belgium (ca. Mindel) Zones before the end of the Pliocene but also during post-Tiglian generally flowed in a north-eastern direction across the (ca. Mindel) time. Deposits belonging to the Kedichem Formation comprise Campine Block. It has to be noted that the well-known Rupel Middle Fine Middle Fine Praeglacial older than Middle Lower Needien Serie of Kedichem material derived from two main and different source areas and Campine cuestas in Belgian did not exist at that time Main Terrace Fine Fine (Mindel-Riss Interglacial) (Gunz- Mindel interglacial) (Mindel-Riss interglacial) (possible Günz & Günz-Mindel (i.e. the Rhine-Meuse river system and rivers that drained the (De Ploey, 1961; Pissart, 1974; Tavernier & De Moor, 1974; Zones interglacial) (Günz to Mindel-Riss (Mindel-Riss central and northern part of Belgium) and interdigitate clearly Vandenberghe & De Smet, 1979; Kasse, 1988). interglacial) interglacial) with deposits of the Tegelen Formation. It is worthwhile mentioning that, according to the definition (cf. Doppert et Late Pliocene and Early Pleistocene fluvial sedimentation Zone of Taxandrien Tiglien Tegelen al., 1975) and mainly determined by their supposed ages, all prograded gradually westwards in the LRE. At the same time (Günz II) (possible prae-Günz) (Günz III three of the formerly defined formations encompass river a progressive shift of the coastline took place in western interstadial) terrace deposits of the Meuse that occur in the southern part and north-western directions. Estuarine depositional of Limburg. conditions predominated in the transitional zone to full Lower Coarse Lower Coarse Serie of Tiglien Sterksel marine environments (Kasse; 1986, 1988). The distribution (Günz & Mindel) (Günz) (Günz I-II interstadial) Because of the reasons above mentioned the authors of these estuarine deposits seems to cover a much larger (ca. Mindel) have carried out a redefinition of the Upper-Pliocene and area than previously thought. In the south-western part of Lower Pleistocene fluvial deposits in the southern part of the Netherlands and in the central part of the RVG marine W Western Netherlands S Southern Netherlands the Netherlands (Weerts et al., 2000; Ebbing et al., 2002; sediments of the Maassluis Formation interdigitate with the Westerhoff et al., 2003). The content as well as the concept Lower Pleistocene fluvial sequences. Future research Figure 2.3a. Lithostratigraphical subdivisions of Pleistocene fluvial deposits by various authors in the first half of the 20th century.
22 23 (1953). This work essentially describes a biostratigraphy the Upper Pliocene and Lower Pleistocene fluvial deposits Zagwijn, 1957, 1958 Zonneveld, 1958 Doppert et al., 1975 Fluvial lithostratigraphy Southern 1960, 1963, 1985 (in: Zagwijn & Van Netherlands [this paper] (Westerhoff of the Pleistocene. It was the first time in the Netherlands respectively into the Kieseloolite, Tegelen and Kedichem Staalduinen, 1975) et al., 2003) that several pollen diagrams were published and used to formations (see also Fig. 2.2). He omitted the various establish a subdivision of the Pleistocene based on stages. terrace deposits of the Meuse in South Limburg from these Chronostratigraphy Meuse Rhine Fluvial deposits Meuse Rhine These authors placed the Reuver Clay in the Late Pliocene formations, as was done later by Doppert et al. (1975). Zonneveld’s lithostratigraphical terminology was also applied Betuwe Formation Echteld Formation Reuverian Stage that later was presented in more detail R + M by Zagwijn (1960). The onset of the Pleistocene Series was by Zagwijn (1960, 1963a) who established the definitions
Holocene defined by these workers as Pretiglian. One should notice that of the lithostratigraphic units in more detail, and also the Weichselian* this Pretiglian (cf. Van der Vlerk & Florschütz, 1953) includes chronostratigraphical subdivision into stages and substages Grubbenvorst Kreftenheye Kreftenheye Formation Kreftenheye all deposits between the Reuver Bed and the Tegelen Clay and that was based on the palynological evidence. Formation Formation R + M Formation Eemian disregards the logical entity of sedimentary fluvial cycles. So, this first definition of the Pretiglian is a purely lithologically 2.4 The newly defined Waalre and Stramproy Late Saalian* defined subdivision. Furthermore Van der Vlerk & Florschütz Formations Veghel Well Sands Formation Vianen Formation (1953) defined a Tiglian Stage, based on their studies of the Holsteinian
Urk Formation Urk Veghel Beegden Formation Urk Tegelen Clay exposed in several excavations in the vicinity of 2.4.1 Introduction Elsterian* Lingsfort Sands Formation Formation Formation Tegelen. The post-Tiglian period was assigned as Taxandrian, In the revised lithostratigraphical system the Upper Pliocene R M a stage that lasted until the Needian. The latter is correlated and Early Pleistocene fluvial deposits in the southern part Sterksel nowadays with the Middle Pleistocene Holsteinian. Apart of the Netherlands are subdivided into two newly defined Cromerian Formation Sterksel complex** Sterksel from studies in exposures, Van der Vlerk & Florschütz (1953) formations. Both formations are situated between the Formation Formation were able to distinguish some of the stages in boreholes. Kieseloolite Formation and the Sterksel Formation. Deposits Enschede
Mid Subsequently, Zagwijn developed this approach in detail by formed by the mixed Rhine-Meuse river system are referred Bavelian** Formation analysing a great number of borehole sequences. Based on this to the Waalre Formation whilst the Stramproy Formation Pleistocene E Menapian* pollen analytical evidence a further subdivision of the Early comprises deposits formed by rivers that drained the central Kedichem Kedichem Pleistocene was established in a number of consecutive stages and northern part of Belgium together with deposits of more Waalian Formation p.p. Formation R + M (Zagwijn, 1957, 1960). local origin. Eburonian* Harderwijk A brief summary of the main characteristics is given below. Formation Incl. local & periglacial dep. periglacial & local Incl. 2.3.4 The (litho)stratigraphy of the Geological Full descriptions can be consulted on the lithostratigraphical E Tegelen Survey (4) pages of DINOloket (www.dinoloket.nl). Several terraceSeveral deposits in South Limburg Early Tiglian Tegelen Formation In the early 1950s the Geological Survey of the Netherlands
Formation R + M deposits in South Limburg Terrace Formation Stramproy (Belgian rivers) Formation Waalre began a new national mapping programme at a 1:50.000 2.4.2 The Waalre Formation (WA) scale. As a consequence, the Geological Survey took a strong The holostratotype of the Waalre Formation is defined in Praetiglian* lead in all types of stratigraphic studies. The main goal was the intervals between 126-144 and 158.60-206 m of borehole to establish a stratigraphic framework that could be applied 51D0343 at Waalre (Fig. 2.1, 2.4). Reuverian Kieseloolite Formation Scheemda Kieseloolite in the mapping programme. Such a system not only required Formation Formation formalisation of lithostratigraphical units, but should also 2.4.2.1 General lithology Kieseloolite Formation E R + M Pliocene provide a reasonable insight in the chronostratigraphical The Waalre Formation deposits consist of a number of stacked subdivision of the Plio-Pleistocene period. For this purpose, fining upward cycles with grain-size variations ranging from the work of Van der Vlerk & Florschütz (1953) and Zonneveld coarse-grained, gravel-bearing sand in the basal parts to clay * Cold R Rhine b M Meuse (1947 ) was taken as a starting point. In particular the first with a low silt content in the upper parts of individual cycles. ** Complex unit composed authors had adopted biostratigraphy as a fundamental Sand forms the dominant lithology but clay layers may be of at least 4 interglacials E ‘Eastern’ rivers and 3 glacials approach in stratigraphy and had abandoned the well-known widespread on a regional scale. Gravel occurs more frequently non-deposition morphostratigraphical subdivisions based on the concepts of in the lower parts of the formation. Generally a decrease of Penck & Brückner (1909). Apart from this, it was believed that the mean grain size can be observed in north-western and Figure 2.3b. (Litho)stratigraphy of Early Pleistocene fluvial deposits in the southern part of The Netherlands (after Zonneveld, 1958; Doppert et al., 1975; Weerts et al., 2000). The table of Zonneveld (1958) was the first lithostratigraphical scheme with a Pleistocene chronology based on the pollen-defined subdivision introduced by Zagwijn (1957). a systematic pollen analytical survey of Quaternary peat and western directions. Locally, dark brown to black thin (< 0.5 m) clay strata could contribute to a detailed biostratigraphical peat layers may occur in the clayey parts of the formation. The subdivision. In numerous outstanding publications Zagwijn sediments are characterised by low to moderate admixtures of (1957, 1960, 1963a,b, 1982; Zagwijn & Zonneveld, 1956) mica flakes, dark-coloured particles in the fine sand fraction, Zagwijn (1960) introduced the stratigraphically more formal Study of fossil molluscs was focussed on marine deposits but elaborated a (bio)stratigraphy for the entire Pliocene and and red-brown components in the coarser grained fractions. terminology laid down by Hedberg (1954) and began using several authors also examined fresh-water assemblages in Early Pleistocene. Below the groundwater table grey colours predominate the formations instead of zones and series. In the same papers the fluvial deposits (e.g. Tesch, 1911, 1928, 1934; Haas, 1920; sandy parts while clay is often blue-grey in colour. the lithostratigraphical units were correlated with a detailed Van Regteren Altena, 1955). Based on fossil plant macro- Doppert & Zonneveld (1955) made the first attempt to chronostratigraphic scheme (Fig. 2.3a, 2.3b). remains, Reid & Reid (1915) were the first who could give a compile a more formal lithostratigraphy by combining the 2.4.2.2 Additional lithological characteristics
firm palaeontological basis for the distinction between the pollen analytical and sediment-petrological evidence. Their The CaCO3 content is highly variable and may range from 2.3.3 The palaeontological approach (3) Reuver Bed (Pliocene) and the Tegelen Clay (Pleistocene). This lithostratigraphical units were named zones and series, 0 to 3 on a relative scale (3 ≥ 1.5-2%). Clay deposits often
During the first half of the last century, palaeontological subdivision in Pliocene and Pleistocene could be confirmed by and ordered into a stratigraphic framework by combining show a high content of siderite (FeCO3). The siderite may be studies had the lead over the stratigraphic research. Regarding later published studies on large and small mammal remains superposition and biostratigraphical evidence. One of the dispersed in the sediments but can also occur in laminated the fluvial deposits in the southern part of The Netherlands (Schreuder, 1943, 1950). Pollen analytical studies (at first important conclusions was that the hitherto Mindel-Riss enrichments, or in the form of nodules. Bioturbation can be much attention was paid to the faunal and floral composition applied in the 1940s) led to similar conclusions (e.g. Florschütz age of the Serie van Kedichem appeared to be older and observed in excavations and undisturbed cores and usually of the clay deposits near Tegelen and Reuver (e.g. Dubois, & van Someren, 1948). could be seen as part of the Early Pleistocene. In a following occurs in fine-grained laminated deposits. In general they 1905; Fliegel & Stoller, 1910; Tesch, 1911, 1928, 1934; Reid & A comprehensive base for the palaeontological subdivision of paper Zonneveld (1958) adopted the formal stratigraphical indicate estuarine depositional conditions. Geophysical well Reid, 1915; Bernsen, 1930, 1930-1932; Schreuder, 1943, 1950). the Pleistocene was published by Van der Vlerk & Florschütz nomenclature of formations (Hedberg, 1954) and subdivided logs (i.e. Gamma Ray) show fairly well the stacked fining
24 25 Lithology Figure 2.4. Lithology, heavy-minerals and lithostratigraphy of borehole 51D0343 %
(near Eindhoven); holostratotype of the Waalre Formation. 3
Grainsize Depth in m Lithology Sedimentology CaCO Org. mat. % Gamma Ray Mica flakes* Glauconite* Molluscs* Lithostratigraphy 0
Lithostratigraphy Depth in m Clay f-m. Sand c. Sand-Gravel Mica flakes Heavy-minerals Boxtel 0 Fm Boxtel Formation
20 WA-3
20
40 Waalre Formation Waalre Sterksel Formation 60 40 WA-2 WA-2
80
60
100 Stramproy Formation Stramproy
120
80 WA-3 WA-3 WA-Fm
140 Oosterhout Formation
Legend Formation Stramproy Lithology 100 160 Peat
WA-2 WA-2 Clay
180 Sand
120 Waalre Formation Waalre Heavy-minerals WA-1 WA-1 200 Garnet
Epidote Breda Formation
220 Saussurite 140 Alterite
Hornblende
Clay Fine Sand Coarse Sand 240 Volcanic minerals 0 20 40 60 80 100% 0 3 0 3 0 3 0 25 50 0 0.4 0.8 1.2 100 cps
Kieseloolite Formation * relative occurrence in % of bulk sample Rest group (stable minerals incl. Zircon, Rutile a.o.) Legend 3 categories: 1-low, 2-moderate, 3-abundant 260 Staurolite Lithology/Sedimentology Grainsize
Metamorphic minerals Mollusc remains Rootlets < 2 mm 105-150 mm 300-420 mm Ooster- hout Fm Tourmaline Fine-grained gravel Clay flasers 2-63 mm 150-210 mm 420-2000 mm 280 0 3 0 20 40 60 80 100% Bioturbation Peat 63-105 mm 210-300 mm
Clay
26 Figure 2.5. Lithology, grain-size distribution, and lithostratigraphy of borehole 49G0204 (near Huijbergen); hypostratotype of the Waalre Formation. 27 upward cycles of the formation. The fluvial fining upward Waalre Formation also includes deposits that were formerly cycles range in thickness between 7-12 m. Thicker sequences attributed to the upper part of the Kieseloolite Formation; up to 20-30 m typify deposition in estuarine environments. i.e. that part typified by Rhine deposits with unstable heavy- The heavy-mineral content of the deposits shows a 90% mineral associations. dominance of unstable heavy-minerals (garnet, epidote, Mixed Rhine-Meuse deposits formerly considered as part saussurite/alterite, hornblende; see also Fig. 2.4). of the Kedichem Formation, cf. Doppert et al. (1975) now form part of the Waalre Formation. Lithologically they do
2.4.2.3 Genesis/sedimentary characteristics, distribution, not show any difference with other Rhine-Meuse deposits North Sea North Sea thickness and age of the Waalre Formation. Their assumed post-Tiglian age is The Waalre Formation includes fluvial and estuarine sediments not a criterion that justifies their assignment into a seperate supplied by the Rhine-Meuse fluvial system. All facies types lithostratigraphic unit. Amsterdam Amsterdam that are characteristic of fluvial and estuarine deposits occur Influxes of coarse-grainedR hine-Meuse deposits formerly Den Haag Den Haag within the formation. As observed in excavations the sand and assigned as the so-called ‘Bunnik Rhine’ influence within Utrecht Utrecht gravel deposits of the Waalre Formation show channel and the Harderwijk Formation (cf. Doppert et al., 1975; see also Rotterdam Rotterdam pointbar facies types. Gravel-bearing channel ‘lag’ deposits Jelgersma & Zandstra, 1970) are now included in the Waalre Venlo Block Venlo Block Roer Valley Raben Roer Valley Raben characterise the lower part of the formation. The fine-grained Formation (see 2.6). Northern Northern Krefelder Block Krefelder Block Eindhoven 49G0204 Eindhoven and clayey deposits of the Waalre Formation exhibit four Peel Block Peel Block Venlo Rhine Venlo Rhine characteristic lithofacies types: 2.4.3 The Stramproy Formation (SY) 51D0343 51D0343
• channel fills, formed in oxbow lakes. They usually consist The holostratotype of the Stramproy Formation is defined LRE LRE Köln Köln of horizontally bedded clay deposits. Thin (cm-dm) sand in borehole 57H058 at Stramproy in the interval between Scheldt Kölner Block Scheldt Kölner Block
layers, often showing climbing ripple structures may 46.50-136.80 m (Fig. 2.1, 2.7). Ruhr Scholle Ruhr Scholle Maastricht Erft Block Maastricht Erft Block occur in between 5-40 cm thick individual clay beds. Local Aachen Aachen Rhenish Massif Rhenish Massif white-coloured enrichment of siderite can accentuate 2.4.3.1 General lithology Meuse Meuse the sedimentary lamination and the amount of siderite The deposits of the Stramproy Formation consist than may increase to values of 90%. When the siderite is predominantly of fine to coarse-grained sand with a high Waalre Formation (subunit WA-1) Waalre Fm. (subunit WA-2) Borehole 49G0204, hypostratotype Waalre oxidised it shows red-brown or rust colours. quartz content. Medium to coarse-grained gravel locally forms Borehole 51D0343, holostratotype Waalre Formation, Waalre Fm. (Tegelen Member) Fm., see figure 2.5 • flood-basin fines: deposits consisting of clay, silt and very thin ‘lag’ deposits. Clay deposits may contain very fine sand see figure 2.4 fine sand formed in the (extensive) flood-basins in between and silt. In the southern part of the distribution area, clay active channel belts. Such clayey deposits have a massive layers are relatively thin and seldom exceed 2 m thickness. In appearance and contain hardly any sedimentary structures. the western part of the distributive area clay layers may occur Locally, thin humic horizons consisting of peat or brown- over vast areas and can reach a thickness of several metres. coal may occur. Sometimes the clay has a crumbly or Thin (< 1 m) dark peat layers in between the sandy deposits prismatic structure as a result of initial soil-forming are irregularly distributed throughout the formation. Humic or processes. peaty horizons may occur sporadically within the clay layers. • crevasse splays and levees, consisting of small scale The sand deposits of the formation are usually light brown
(cm-dm) alternations of fine-grained sand and clay. to light white-grey in colour. The clay is generally olive grey to North Sea North Sea • estuarine and/or lagoonal clay deposits, consisting of brown grey. clay with a variable content of silt and very fine sand.
Locally thin peat layers may occur in the uppermost part. 2.4.3.2 Additional lithological characteristics Amsterdam Amsterdam The transition to underlying sandy deposits is always For the larger part the sediments of the Stramproy Formation Den Haag Den Haag characterised by strongly alternating bedding of thin lack carbonates, although there may be some local exceptions. Utrecht Utrecht sandy and clayey strata (Fig. 2.5). Humic soil horizons may occur repeatedly in the formation, Rotterdam Rotterdam especially in the sandy deposits of the southern part of the Venlo Block Venlo Block Roer Valley Raben Roer Valley Raben The distributional area of the Waalre Formation is shown in RVG. Parts of the formation are also affected by cryoturbation, Northern Northern Krefelder Block Krefelder Block figure 2.6. Due to erosion the formation is absent on large frost wedges and other periglacial phenomena. 49G0204 Eindhoven Peel Block Peel Block Venlo Rhine Venlo Rhine Eindhoven parts of the Peel Block area. The thickness varies from a few In geophysical well logs the sandy parts of the formation are 51D0343 57H0058 metres on the Peel Block to over 90 m in the RVG. The Waalre characterised by a very low response of the Gamma Ray curve LRE Köln LRE Köln Formation is of Late Pliocene to Early Pleistocene age. (Fig. 2.7). Scheldt Kölner Block Scheldt Kölner Block
The heavy-mineral content of the formation is dominated by Ruhr Scholle Ruhr Scholle Maastricht Erft Block Maastricht Erft Block 2.4.2.4 Subdivisions 90% of stable minerals (e.g. zircon, staurolite, metamorphic Aachen Aachen Only one member is defined formally within the formation: minerals and tourmaline). Rhenish Massif Rhenish Massif Meuse Meuse the Tegelen Member. This Tegelen Member comprises the remnants of the Waalre Formation on the Peel Block. 2.4.3.3 Genesis/sedimentary characteristics, distribution, Waalre Formation (subunit WA-3) Stramproy Formation 0 25 50 km thickness and age Waalre Formation (Tegelen Member) Major fault 2.4.2.5 Relation to previously defined units The deposits of the Stramproy Formation comprise a wide Borehole 57H0058, holostratotype Stramproy Formation, With the exception of the Early Pleistocene terrace deposits range of fluvial, estuarine, periglacial, and aeolian facies Interfingering of Waalre Formation and Peize Formation see figure 2.7 of the Meuse in South Limburg the Waalre Formation types. The larger part of the formation consists of fluvial encompasses the deposits of the Tegelen Formation cf. facies related to the fluvial systems that drained the central Doppert et al. (1975). The Early Pleistocene terrace deposits and northern part of Belgium. To the west and northwest of the Meuse are now incorporated into the Beegden estuarine facies types become increasingly important. Local Figure 2.6. Distributional area of the deposits of the Waalre and Stramproy Formations: A) distribution of the WA-1 deposits (equivalent to the Oebel Beds), B) distribution of Formation (Weerts et al., 2000; Westerhoff et al., 2003). The and aeolian deposits are irregular distributed and mainly the WA-2 deposits; D) distribution of the WA-3 deposits; D) distribution of the deposits of the Stramproy Formation.
28 29 Lithology Figure 2.7. Lithology, Gamma Ray curve, heavy-minerals and lithostratigraphy formed under periglacial environmental conditions. by 6-10 m thick clay strata characterise the Kieseloolite of borehole 57H0058 (near Stramproy); the holostratotype of the Stramproy The maximum distributional area of the Stramproy Formation Formation in the southern part of the RVG (Figs, 7, 8, 9). The Formation (see Fig. 2.4 for legend heavy-minerals). is the RVG, the area immediately to the west, and parts of clay strata show repeated intercalations of peat and brown the Western Netherlands (Fig. 2.6). Except for a relatively coal. The vertical lithological composition is clearly expressed Mica flakes Glauconite Heavy-minerals Gamma Ray Lithostratigraphy Depth in m Clay f-m. Sand c. Sand Gravel
0 small area along the Dutch-German border near Venlo, the in Gamma Ray logs: increasing values for the clayey deposits Boxtel Fm. formation is absent on the larger part of the Peel Block area. and relatively low values for the sandy parts. At the top of the The thickness varies from less than 1 m to about 100 m in the formation a widespread and easily-mapped clay layer occurs. southern part of the RVG. It always shows a Reuverian type pollen assemblage and is 20 lithostratigraphically assigned to the Reuver Bed (Reid & Reid, The Stramproy Formation is Early Pleistocene in age. Based 1915: Zagwijn, 1960; Boenigk & Frechen, 2006). on its stratigraphic position (Fig. 2.8), it is concluded that The lowermost part of the formation in the southern part of
Sterksel Formation parts of the formation are formed concurrent with the Waalre the RVG might form the northern continuation of the so-called 40 Formation. This implies that the age of its lower boundary Indener Schichten (indicated by the dashed line in Figs. 2.8, is older than generally believed for the former Kedichem 2.9) which is thought to be of Late Miocene age (Schäfer et al., Formation (Westerhoff et al., 2008). 2005).
60 2.4.3.4 Subdivisions The main source area of the deposits occurs in the pre- Thus far, the Stamproy Formation has not been subdivided Rhine drainage basin (Boenigk, 1978a; Gliese & Hager, 1978). into members status units. Upstream of the confluence with the Meuse the Kieseloolite
80 Formation consists of pure pre-Rhine deposits with some 2.4.3.5 Relation to earlier defined units admixtures of local tributaries (Kemna, 2005, 2007). The Stramproy Formation comprises those parts of the former Downstream of the confluence the formation consists of Kedichem Formation (cf. Doppert et al., 1975) that were not mixed pre-Rhine and Meuse deposits with some admixture 100 deposited by the Rhine-Meuse system. of material supplied by the Belgian rivers. Stramproy Formation Stramproy All deposits supplied by these river systems are typified by 2.5 Characterisation of the Upper Pliocene and Lower a high quartz content and dominantly stable heavy-mineral Pleistocene fluvial deposits in the southern part of associations. As a result, deposits of the Meuse and Belgian 120 the Netherlands, with regard to their provenance and rivers cannot be mapped separately from pre-Rhine deposits. sedimentary facies Only a slightly higher amount of metamorphic minerals may The Pliocene and Lower Pleistocene fluvial deposits in the indicate that the Meuse and/or the Belgian rivers contributed southern part of the Netherlands are derived from different sediment to the Kieseloolite Formation. Locally, an increase 140 sources: the pre-Rhine and Rhine drainage system, the Meuse, of Meuse influence can be distinguished from Rhine deposits and a system of consequent rivers that drained the central by increasing values of flint and quartz in the gravel fraction and northern part of Belgium (Fig. 2.1). (Boenigk, 1970, 2002). Terrace deposits of the Meuse in
160 Together these major river systems have formed an extensive the East Meuse Valley in southern Limburg are included wedge of alluvial sediment in the southern part of the North lithostratigraphically in the new defined Beegden Formation Sea Basin. The petrographical composition of the deposits is that comprise all pure (i.e. not mixed with Rhine) Meuse controlled by their provenance. Lithology and sedimentary deposits (Weerts et al., 2000; Westerhoff et al., 2003). 180 characteristics of the deposits reflect the depositional The deposits of the Kieseloolite Formation were formed in conditions which are largely determined by climate and a vast lowland area that was situated near the coast and had tectonic forcing. a generally low gradient. Deposition of the thick clay strata The spatial relationships of the lithostratigraphical units can and intercalated peat took place in extensive floodbasins 200 be mapped over a large area and form the basis of further where peat accumulated in swamps and back-barrier areas. unravelling of the fluvial history in the area. It is likely that their formation was promoted by regional high The outlines of the revised lithostratigraphic framework sea-level stands.
Kieseloolite Formation in the southern part of the Netherlands are illustrated by a 220 Legend few example cross-sections (Figs. 2.8, 2.9, 2.11) and will be 2.5.2 Late Pliocene and Early Pleistocene Rhine- Lithology discussed below. Meuse sequences During the Late Pliocene the catchment of the Upper Rhine Peat 240 2.5.1 The Pliocene fluvial record extended southwards into southern Germany and the Alpine Clay The first fluvial deposits formed in the LRE were derived foreland. As a result, the petrographic composition of the from the strongly weathered overburden of the Rhenish Rhine sediments deposited in the LRE changed drastically. Sand, not differentiated Massif and are assigned to the Kieseloolite Formation. In (Boenigk, 1970, 2002; Boenigk et al., 1972; Hagedorn, 2004; 260 general they consist of light coloured, medium to coarse- Hagedorn & Boenigk, 2008; Kemna, 2007, 2008). This can be Mica flakes, Glauconite grained sands and some gravel. The sediments show a high seen macroscopically by the abundance of mica flakes 3 categories: 1-low percentage of quartz and a dominant stable heavy-mineral (i.e. muscovite), feldspar grains, some red-brown components, Breda 2-moderate content (e.g. Fig. 2.7, the interval between 136.8-277.0 m). the higher carbonate content in the assemblages, and the Fm. 280 0 3 0 3 0 50 100% 0 20 40 CPS 3-abundant The Kieseloolite Formation reaches a thickness of about 200 generally grey colour of the deposits. The marked change in m in the southern part of the RVG (Figs. 2.8, 2.9) but thins out petrographic composition is also well-demonstrated by an towards the northwest in the vicinity of ’s Hertogenbosch. almost complete shift to a 90% dominance of unstable heavy- Sand bodies, up to several tens of metres thick, interrupted minerals (e.g. garnet, epidote, alterite/saussurite
30 31
1 1 1’ 1’
SE SE NW NW
2 2
1 1 1
9 1 0 9 0
5 5
6 5 5 6 9 8 9 8
7 1 7 1
3 3
9 9 9
1 9 9 1 9
5 5
9 0 0 9 9 9 9 9
5 2 5 2
3 3
1 1 2
3 2 1 3 1
0 0
2 1 1 2 0 0 0 0
0 1 0 1
0 0
0 0 0
0 0 0 0 0
0 0
0 0 0 0 0 0 0 0
0 0 0 0
A A
B
F F D B D A A
C C C
B B F F B B C C C C C
1 1
1
7 7 1 1 1 1 1 5 5 5 0 0 7 7 1 1 5 5 5 5 5
Depth in m Depth in m
58D0688
58D0688 51G0550 51G0550
51B0295 51B0295 58D0885 58D0885 51G0306
60B0123 60B0123 57F0062 57F0062 51G0306 58A0089 58A0089 57E0076 57E0076
5 5
5
5 5 5 5 5
51D0199
51D0199 Depth in m Depth in m
51G0271 51G0271
58A0087 58A0087 51G0218 51G0218 5 5
4 4 44F0236 44F0236 4 4 45C0161 6 6 5 5 5 5 45C0161 4 4 4 4 30 30 Boxtel Fm. Boxtel Fm. 30 30 Beegden Formation Beegden Formation 0 0 0 0 Kreftenheye Fm. Kreftenheye Fm. NAP NAP Sterksel Sterksel NAP NAP Formation Formation -50 -50 -50 -50 Stramproy Formation Stramproy Formation
-100 -100 -100 -100 WA-2 WA-2 WA-3 WA-3 WA-1 WA-1 -150 -150 -150 -150 Maassluis Maassluis WA-2 WA-2 Formation Formation -200 -200 -200 -200 Kieseloolite Formation Kieseloolite Formation
-250 -250 -250 -250
Inden Formation? Inden Formation? ? ? -300 -300 -300 -300 Oosterhout Formation Oosterhout Formation -350 -350 -350 -350
-400 -400 -400 -400 Breda Formation Breda Formation -450 -450 -450 -450
-500 -500 -500 -500
Legend Legend 0 10 km 0 10 km NAP: Dutch ordinance datum ≈ mean seaNAP: level Dutch ordinance datum ≈ mean sea level Borehole lithology Borehole lithology Heavy-minerals Heavy-minerals
Peat Coarse sandPeat Coarse sand Garnet Alterite Garnet RestAlterite group (stable minerals incl. Zircon, RestRutile group a.o.) (stable minerals incTourmalinel. Zircon, Rutile a.o.) Tourmaline
Clay Gravel and Claygravel bearing coarse sand Gravel and gravel Epidotebearing coarse sand HornblendeEpidote StauroliteHornblende Staurolite
Fine sand Shell rich CragFine sand Shell rich Crag Saussurite Volcanic Saussuriteminerals MetamorphicVolcanic minerals minerals Metamorphic minerals
Figure 2.8. Cross-section 1-1’ (see Fig. 2.1) in the Roer Valley Graben showing the Pliocene and Pleistocene lithostratigraphical units. Based on lithology of boreholes, heavy-mineral data, and gamma-ray curves. Note that remnants of the WA-1 unit occur in the southern as well as in the northern part of the RVG.
and hornblende, see also Fig. 2.4, at about 210 m). (Figs. 2.8, 2.9). They are also known from the Brachterwald Within the RVG the occurrence of the WA-1 subunit is limited (> 40 m) of subunit WA-2 is shown. The basal part consists Downstream of the Rhine-Meuse confluence nearJ ülich area (east of Tegelen) on the Peel Block (i.e. the pits near to the tectonically deepest parts (Figs. 8, 9; Michon et al. 2003) of 20-30 m thick channel deposits that are overlain by these Rhine deposits are mixed with sediment supplied by Oebel and Hoher Stall; Boenigk 1970, 1978b; Kemna 2005, and can be traced from the Dutch-German border area to the floodbasin fines. At least two fluvial fining-upward cycles the Meuse. However, being the larger river, the sediments 2008; Westerhoff, 2004, chapter 4). Generally they consist of a vicinity of Eindhoven (Fig. 2.6). Here, in the Waalre borehole are observed in the northern part of the RVG. Apart from the of the Rhine dominate the Meuse influence in the complete fining-upward cycle of fluvial deposits with a gravel- (Fig. 2.4) the heavy-mineral content shows fairly well the relative small areas where remnants of subunit WA-1 occur assembled deposits. This effect is even more important in bearing basal part and a thick clay layer at the top. The clay marked change from stable to unstable associations. Isolated the WA-2 subunit is underlain by deposits of the Kieseloolite the heavy-mineral composition because Rhine sediments usually shows two or more peat or browncoal intercalations. finds of deposits of subunit WA-1 in the southern part of the and Oosterhout Formations. At the western and north-western contain a considerable higher amount of heavy-minerals The thickness of the unit varies between 15-25 m. RVG and the adjacent area of Germany indicate that after its distribution limit the deposits of subunit WA-2 gradually when compared to Meuse deposits (Zonneveld, 1947b, The Reuver Bed forms a marked clay deposit with intercalated deposition intensive erosion may have taken place (Kemna, grade into shallow marine and near-coastal deposits of the 1950). Generally, the contribution of Meuse sediment can brown coal layers at the top of the Kieseloolite Formation 2005, 2008; Westerhoff et al., 2008). The currently known area Maassluis Formation. In a zone along the Belgian border, be recognised only in the gravel fraction (Kurtz, 1913; and is overlain by subunit WA-1. The latter shows a fining- of occurence (Fig. 2.6) must be seen as a minimum. The poorly west of the RVG, marine deposits of the Maassluis Formation Boenigk, 2002). The mixed Rhine-Meuse deposits which are upward trend with a floodbasin clay at the top. Subunit described lithology in several (older) borehole data often are repeatedly intercalated within estuarine/fluvial deposits characterised by unstable (Alpine) heavy-minerals overlie the WA-1 is overlain by gravel-bearing deposits of subunit hampers the possibilities for an adequate recognition of the of subunit WA-2. These marine intercalations show rather Kieseloolite Formation and are lithostratigraphically assigned WA-2 that characterise an unconformity which has been deposits of subunit WA-1. irregular distribution patterns and therefore they cannot be to the Waalre Formation. In the RVG three subunits of the observed in large parts of the LRE (Boenigk, 2002; Boenigk mapped individually on a regional scale or subdivided into Waalre Formation, respectively labelled WA-1, WA-2 and & Frechen, 2006). Due to the lithostratigraphic position and The gravel-bearing basal part of subunit WA-2 marks an separate lithostratigraphical units. WA-3, can be distinguished from bottom to top (Figs. 2.4, 2.8). the characteristics of the deposits the WA-1 subunit can be erosional boundary that can be traced in the RVG and large correlated with the so-called Oebel Beds that are known from parts of the LRE. In the southern part of the RVG subunit The uppermost part of the Waalre Formation, subunit WA-3, The lowermost deposits of the Waalre Formation are typified several sites in the LRE (Boenigk, 2002; Heumann & Litt, WA-2 consists of a fluvial fining-up cycle with a thickness is well-developed in the northern part of the RVG and can by a marked change in petrography and show the increase 2002; Kemna, 2005, 2007, 2008; Boenigk & Frechen, 2006;). of 10-15 m (Figs. 2.8, 2.9). Here, in the most subsided part also be found in the area west of the RVG (Fig. 2.6, 2.8, 2.10). to a nearly full dominance of unstable heavy-mineral The clay deposits of subunit WA-1 contain Reuverian-type the subunits WA-1 and WA-2 are separated by an intercalation The deposits of subunit WA-3 consist of a number of stacked associations (Fig. 2.4). These deposits are indicated as subunit pollen assemblages (Boenigk, 1970, 2002; Zagwijn 1974; of deposits of the Stramproy Formation (Fig. 2.9). In the fining-upward cycles. In comparison with subunits WA-1 and WA-1 and are found in several boreholes in the RVG Westerhoff, 2004) which confirms their Late Pliocene age. northern part of the RVG a much thicker accumulation WA-2 the basal parts of the depositional cycles of subunit
32 33 WA-3 have a considerable lower mean grain size and contain the mixed Rhine-Meuse deposits of the WA-3 subunit catchment and flowed across the Campine Block towards 2.6 Discussion hardly any gravel. Thick clay deposits (> 6 m) formed in interdigitate with the Peize Formation (Weerts et al., 2000; the RVG (Tavernier & De Moor, 1974; Kasse, 1988). As soon extensive floodbasins characterise the topmost depositional Westerhoff et al., 2003). The latter consists of fluvial deposits as these rivers entered the Rhine-Meuse floodplain their 2.6.1 Stratigraphical position of the Waalre and cycle of the WA-3 subunit in the RVG and the adjacent area supplied by the Eridanos fluvio-deltaic system that drained sediments became intermingled with those of the Rhine- Stramproy Formations west of it. Their occurrence is widespread throughout the the Baltic area during a large part of the Neogene and Meuse. Due to the lithological overprint of the Rhine-Meuse, The deposits of the Rhine, Meuse, and Belgian rivers form study area. The maximum thickness of the WA-3 subunit in Quaternary (Bijlsma 1981; Overeem, 2002). In the western part the deposits of the Belgian rivers can no longer be recognised an extensive wedge of Pliocene and Quaternary deposits in the RVG can amount up to 80 metres. of the Netherlands deposits of the Waalre Formation may also separately. So, the deposits of the Belgian rivers can only be the southern part of The Netherlands. Three main features of overlie the Peize Formation (Fig. 2.10). mapped when they are not mixed with Rhine-Meuse material. stratigraphical significance in this depositional sequence can In the RVG a clear break exists between subunit WA-2 and The deposits of the Stramproy Formation consist of fine to be recognised and traced over a large part of the area: WA-3. It is well-expressed by intercalating deposits of the 2.5.3 Deposits of the Belgian rivers medium-grained quartz-rich sand and are dominated by a • the marked change in petrography between the pre-Rhine Stramproy Formation at a depth of about 140-160 m near Fluvial systems that drained the central and northern part stable heavy-mineral content (borehole Stramproy, Fig. 2.7). deposits (typified by stable heavy mineral associations) Eindhoven (2.8). Further to the North marine mollusc-bearing of Belgium form the third main sediment source of the The near absence of well-developed thick clay layers in the and the (Alpine) Rhine deposits (typified by unstable heavy deposits of the Maassluis Formation interdigitate with Lower Pleistocene fluvial deposits in the southern part of the southern part of the RVG is noteworthy. Here, the Stramproy mineral associations). subunits WA-2 and WA-3. Netherlands. Lithostratigraphically their deposits are assigned Formation can reach a thickness of 80-90 m. The (local?) • the erosional boundary at the transition from Upper North of the distribution limit of subunit WA-2 (Fig. 2.6) all to the Stramproy Formation. During the Early Pleistocene intercalation of the Stramproy Formation in between subunits Pliocene to Lower Pleistocene deposits. deposits of subunit WA-3 are underlain by the Maassluis a system of southwest to northeast orientated consequent WA-1 and WA-2 of the Waalre Formation (Fig. 2.9) indicates • the ealisly-mappable coarse-grained gravel-bearing Formation. In the central and western part of The Netherlands rivers drained the eastern part of the present-day Scheldt a temporarily diminished influence of the Rhine in the base of the Sterksel Formation which represents a major southern RVG after the deposition of subunit WA-1. Similar unconformity that occurs over large parts of the LRE influxes of material from the Stramproy Formation are found (Boenigk & Frechen, 2006). in the Waalre Formation at the Brachterwald area (Boenigk, Figure 2.9. Cross-section 2-2’ (see Fig. 2.1) in the southern part of the RVG showing the Pliocene and Pleistocene lithostratigraphical units. Based on lithology of boreholes, 1970; Kemna, 2005, 2008; Westerhoff et al., 2008). As stated The Waalre Formation occurs between the marked change heavy-mineral data, and gamma-ray curves. Legend see Fig. 2.8. above the presence of such well-recognisable deposits of the in petrography and the regional unconformity at the base of Stramproy Formation can only be explained by absence of the the Sterksel Formation (Fig. 2.11). The Stramproy Formation 2 2’ Rhine-Meuse river system. A main cause for this can be sought is positioned between the erosional boundary at the top of SW NE in shifting positions of the main active stream belts of the the Upper Pliocene deposits and the regional unconformity at 57H0058 57H0107 57H0069 58A0165 58A0095 58A0087 58A0039 58A0166 58B0123 58B0030 58B0189 40 40 Rhine-Meuse system. As the Rhine-Meuse system disappears the base of the Sterksel Formation. The distinction between Boxtel Fm. from the southern RVG the available accommodation space the two formations primarily depends on their differences in Beegden Fm. can be filled by material supplied by the Belgian rivers. provenance. 0 0 NAP Sterksel Formation NAP Compared to the former Tegelen Formation (cf. Doppert et al., In the transitional zone from the southern to northern 1975), the lower and upper boundary of the Waalre Formation RVG (between Asten and Eindhoven) the deposits of the are not determined by pollen-defined substages (i.e. Reuverian -50 -50 Stramproy Formation Stramproy and Waalre formations seem to interdigitate. and Early Eburonian) but by a clear lithostratigraphical A major intercalation of the Stramproy Formation which position that is distinguished using easily-mapped major subdivides the WA-2 and WA-3 subunits, is mapped in the changes in lithology. -100 -2 -100 WA vicinity of Eindhoven and northwards. (Figs. 2.4, 2.8). Here, it also indicates a temporary interruption of Rhine- 2.6.2 Waalre Formation A -1 W Meuse sedimentation. Deposits of the Stramproy Formation The threefold subdivision of the Waalre Formation that can -150 Kieseloolite Formation -150 also interdigitate with deposits of the Waalre and Maassluis be mapped over a vast area and forms an essential element formations in the area west of the RVG (Fig. 2.10). Here, the for reconstructing a regional lithostratigraphic framework. northwards fluxes of the deposits of the Stramproy Formation It shows a rather consistent picture of the stratigraphic -200 -200 seem to be directly related to lower sea levels during glacial sequences preserved in the different areas as defined by OO Fm. periods (Kasse, 1988, 1990; Kasse & Bohncke, 2001). tectonic structures (Fig. 2.11). 0 100% ? -250 -250 The uppermost part of the Stramproy Formation overlies 2.6.2.1 Subunit WA-1 0 100% ? Inden Formation the deposits of the Waalre Formation (WA-3) in the northern The lowermost subunit WA-1 is found in the tectonically deep part of the RVG, on the Peel Block, and the area to the west parts of the RVG (Fig. 2.6) and locally on the Peel Block south -300 -300 of it. This upper part of the Stramproy Formation shows a of Tegelen. The subunit can be correlated positively with considerable thickness near the fault junctions just south the so-called Oebel Beds of Kemna (2005, 2008) and Boenigk of Eindhoven. Further to the North and West deposits of & Frechen (2006). Isolated finds of WA-1 deposits south of -350 Breda Formation -350 the Stramproy Formation consist generally of one or two Roermond may point to tectonically (NE tilting) induced fining-up cycles which end in thick clay layers formed erosion after its deposition. This agrees closely with the
0 100% in extensive flood-basins. The Stramproy Formation is observations made by Boenigk & Frechen (2006). -400 -400 widespread in the southern and western part of the The strong lithological resemblance of the uppermost Netherlands (Fig. 2.6). clay deposit of subunit WA-1 or the Oebel Beds with the Reuver Bed of the Kieseloolite Formation has for a long time -450 -450 hampered a formal distinction between these deposits Depth in m 0 5 km Depth in m (Kemna & Westerhoff, 2007). Consequently the traditionally defined Reuver Bed often includes the equivalent deposits Fault NAP: Dutch ordinance datum ≈ mean sea level of the Oebel Beds or WA-1 subunit. Holostratotype Stramproy Formation Kemna (2005, 2008) assigns the by stable heavy-mineral OO Fm. Oosterhout Formation associations typified Reuver Bed as Reuver Bed s.s..
34 35 3 3 3’ 3’ Putte Putte Zegveld Zegveld SW SW NE NE 49G0191 49G0204 49E0065 49G0191 49E0282 49G0204 49E0065 43H0061 49E0282 43H0063 43H0061 43F0017 43F0091 43H0063 38C0384 43F0017 43F0091 38D0262 38D0108 38C0384 38A0239 38D0262 38A0148 38D0108 38A0239 31D0010 38A0148 31D0160 31D0010 31D0160
WA-3 WA-3 0 m 0 m 0 m 0 m NAP NAP Echteld Fm. Echteld Fm. NAP NAP WA-2 WA-2 Kreftenheye Fm. Kreftenheye Fm. Urk Fm. Urk Fm. Stramproy Fm. Stramproy Fm. Sterksel Fm. Sterksel Fm. Waalre Formation Waalre Formation 50 50 50 50
0 100% 0 100% 0 100% 0 100% 0 100% 0 100% 0 100% 0 100%0 100% 0 100% 0 100% 0 100% Peize Formation Peize Formation -100 -100 -100 -100 0 100% 0 100% Oosterhout Formation Oosterhout Formation
0 100% 0 100% -150 -150 0 100% 0 100% -150 -150
Maassluis Formation Maassluis Formation 0 100% 0 100% -200 -200 -200 -200
-250 Rupel Formation-250 RupelBreda Formation Formation Breda Formation -250 -250
-300 -300 -300 -300
0 100% 0 100%
-350 -350 -350 -350
Fault Fault 0 10 km 0 10 km
Hypostratotype Waalre Formation Hypostratotype Waalre Formation NAP: Dutch ordinance datum ≈ mean seaNAP: level Dutch ordinance datum ≈ mean sea level
Figure 2.10. Cross-section 3-3’ (see Fig. 2.1) west of the Roer Valley Graben showing the Pliocene and Pleistocene lithostratigraphical units. Based on lithology of boreholes, heavy-mineral data, and gamma-ray curves. Legend see Fig. 2.8.
Subsequently he describes the combined sequence of Reuver Block (Boenigk, 1970, 2002; Westerhoff, 2004; Kemna 2005, intercalations of other material are observed in the Waalre Bogemans 1999). Due to erosion during the estuarine Bed s.s. and Oebel beds as Reuver Bed s.l.. However, the 2007; Westerhoff et al., 2008). deposits on the Peel Block, a further subdivision cannot be depositional events, the remaining deposits show an irregular deposits of subunit WA-1 (Oebel Beds) have all characteristics made here. Therefore the deposits of the Waalre Formation and patchy distribution pattern. As a result it is impossible to of the Alpine-influenced Rhine deposits (Boenigk, 2002; 2.6.2.2 Subunit WA-2 on the Peel Block are assigned to the Tegelen Member. So map these individual alternations in the sedimentary record Boenigk & Frechen, 2006). The latter authors therefore Subunit WA-2 has a clear lithostratigraphical position in the far, there is no strong evidence to equate the deposits of on a regional scale. This is the main reason why individual included the Oebel Beds into the lower part of the former RVG (Fig. 2.11). Its lower boundary is marked by an erosion the Tegelen Member to one of the subunits of the Waalre sediment wedges have not been designated to formally Tegelen Formation. This corresponds with the subdivision boundary and the subunit is underlain by clearly identifiable Formation as observed in the RVG. defined lithostratigraphic units. For example, as demonstrated presented here as the lowermost unit of the Waalre Formation. lithostratigraphical units like subunit WA-1, the Kieseloolite by Bogemans (1999), the Hogerheide Member (cf. Kasse, 1988) However, we prefer to use the term Reuver Bed in stead of or Oosterhout formations (Fig. 2.8, 11). At the northern distribution limit, the deposits of subunit is just one of the clayey units of the fluvial/estuarine record of ‘Reuver Clay’ for the topmost clay deposit of the Kieseloolite In the southern part of the RVG subunit WA-2 is relatively WA-2 interdigitate and grade into estuarine facies types the Waalre Formation (Kempen Group in Belgium, Gullentops Formation. In the Netherlands’ lithostratigraphical system, thin and is overlain by a thick sediment body of the Stramproy which eventually continue as shallow marine deposits of et al., 2001) and reflects just one of the periods in which a provenance and related lithological characteristics form Formation (Figs. 2.8, 2.9). This indicates that as soon as the Maassluis Formation (Figs. 2.9, 2.10, 2.11). relatively high sea-level occurred during the Early Pleistocene. the main criteria for the definition of lithostratigraphical the Rhine-Meuse system abandoned the southern RVG the In the area west of the RVG subunit WA-2 can be traced in In the northern part of the RVG subunit WA-2 is overlain units (Weerts et al., 2000; Westerhoff et al., 2003). From that sediment infill was taken over by the Belgian rivers (e.g. a zone along the Belgian border. Here an increasing marine by a wedge of fluvial sediment of the Stramproy Formation it is clear that subunit WA-1 forms an entity with Alpine- Boenigk, 2002; Kemna 2005, 2007; Westerhoff et al., 2008). influence is indicated by a number of intercalations of the that originates from south-westerly directions. At the same influenced Rhine deposits and therefore it cannot be included The much thicker deposits of subunit WA-2 in the northern Maassluis Formation. In the same area repeated influxes of level a wedge of marine deposits belonging to the Maassluis within the Kieseloolite Formation. Future mapping might lead part of the RVG are supplied by a course of the Rhine that material of the Stramproy Formation are also seen in the Formation protrudes from northwestern directions (Fig. 2.8). to a formal definition of subunit WA-1 as a member of the flowed across the Peel Block via the Venlo-Tegelen area Lower Pleistocene sequence (Fig. 2.10). The alternations of A similar situation occurs in the area west of the RVG Waalre Formation. Apart from the occurrence of subunit (Westerhoff et al., 2008). Remnants of the Waalre Formation fluvial deposits of the Stramproy Formation and estuarine (Fig. 2.10). Here the lowermost deposits of the Waalre WA-1 in the RVG deposits of the subunit are also known from on the Peel Block demonstrate the existence of fluvial activity deposits of the Waalre and Maassluis formations reflect Formation are tentatively correlated with the WA-2 subunit the area south of Tegelen. This indicates that the Late Pliocene of the Rhine not only in the area near Tegelen but also in the Early Pleistocene relative sea-level changes and related because of their corresponding lithostratigraphical position. Rhine-Meuse system flowed both in the RVG and on the Peel area to the west of the present Meuse (Fig. 2.6). Since no major climate change (Kasse, 1988, 1990; Kasse & Bohncke, 2001; The deposits show a full estuarine development and part of
36 37 them were formerly classified as the Hoogerheide Member 2.6.2.3 Subunit WA-3 2.6.2.4 Relation to the Peize Formation the WA-3 subunit (Fig. 2.8). (Kasse, 1988, 1990). The influence of material supplied by Subunit WA-3 forms the uppermost part of the Waalre In the central part of the Netherlands the Rhine-Meuse system • the third group of deposits is characterised by a the Belgian rivers is rather high as is shown by the relatively Formation and can be distinguished in the northern part of met the southern lobes of the Eridanos fluvio-deltaic system predominance of estuarine facies types and occurs in high frequency of stable heavy-minerals in these sediments the RVG and the area west of it. The lower boundary is marked and its deposits laterally grade into the Peize Formation the area west of the RVG and the western part of The (Fig. 2.10). However, the intercalations of pure material of the by the intercalations above mentioned of the Stramproy (Fig. 2.10; Westerhoff et al., 2003). The deposits of the latter Netherlands. Stramproy Formation has suffered from erosion and remnants Formation (Figs. 2.8, 2.10, 2.11) and the Maassluis Formation. in that area dominate the general lithological composition. Based on the stratigraphical position in the southern part are only locally preserved. A main intercalation of deposits of Over large parts of the southern and western Netherlands it These characteristic Rhine-Meuse elements are found locally of the RVG it can be concluded that the lower part of the the Stramproy Formation in the Lower Pleistocene sequence is overlain by deposits of the Stramproy Formation (Fig. 2.8, as coarse-grained gravel components in the Peize Formation. Stramproy Formation was deposited concurrently with the west of the RVG is correlated with the Beerse Member in 2.10) The uppermost part of the Waalre Formation extends far Furthermore the Rhine-Meuse influence can be seen regularly subunits WA-2 and WA-3 in the northern part of the RVG Belgium (Kasse, 1988, 1990; Gullentops et al., 2001, Kasse & into the western and even north-western part of the country in the heavy mineral composition of the deposits of the Peize (Fig. 2.8). This observation strongly contradicts the concept Bohncke 2001). This deposit typified by periglacial phenomena (Fig. 2.6). The formerly described Woensdrecht Member Formation (chapter 6). However, pure Rhine-Meuse deposits of the former Kedichem Formation (cf. Doppert et al. 1975). overlies the WA-2 subunit. To the northwest the deposits of (Kasse, 1988, 1990) forms part of the uppermost deposits are present at the top of the Peize Formation in the central The latter unit was thought to have been formed during subunit WA-2 interdigitate with the marine deposits of the of the Waalre Formation in the south-western part of the and western part of the Netherlands. This indicates that the post-Tiglian times on top of the Rhine-Meuse sequence of the Maassluis Formation. A comparable interfingering of subunit distribution area (Fig. 2.10). south-western influence of the Eridanos system came to an former Tegelen Formation. WA-2 and the Maassluis Formation is found in the northern end and the Rhine-Meuse system shifted from its southern In addition, deposits of the Stramproy Formation overlie part of the RVG (Fig. 2.8, chapter 6). positions to a more north-westwards direction. subunit WA-3 in the larger part of the southern Netherlands (Figs. 2.8, 2.10). These uppermost deposits of the Stramproy 2.6.2.5 Relation to former subdivisions of the Lower Formation have a distribution area that extends into the Pleistocene Rhine-Meuse deposits central and western part of the country (Fig. 2.6, 2.10). Their The Woensdrecht, as well as the Hoogerheide Member development results from a (gradual) shift to the northwest Figure 2.11. Lithostratigraphical scheme of the position and stratigraphical interrelationship of the Waalre and Stramproy Formations. (Kasse, 1988), are not retained in the Waalre Formation. of the main pathway of the Rhine-Meuse system. As a result Although both members can be distinguished in vertical stream belts of the Rhine-Meuse system abandoned the areas sections their lateral mappability at a regional or larger scale of the northern RVG and the adjacent Peel Block. Subsequently, Roer Valley Graben Peel Block Roer Valley Graben Northwest of Roer Valley Graben is limited because of a gradual lateral change into other the existing accommodation space in the central and western southern part northern part facies types. This hampers their use in a lithostratigraphical part of the Netherlands was filled with deposits supplied by SE NW S N S N SW W framework for numerically designed subsurface models. Belgian rivers. These shifts of the depositional domains of the Stratigraphy The four members defined within the former Tegelen two river systems (Rhine- Meuse and Belgian rivers) make it Holocene Formation (i.e. Belfeld Gravel and Belfeld Clay and Tegelen likely that the age of the deposits of the Stramproy Formation
Upper Pleist. Gravel and Tegelen Clay; Zagwijn, 1963a, Doppert et al., become progressively younger towards northwest. 1975) are also not retained in the Waalre Formation. The main reason is that distinction could only be made by pollen 2.7 Conclusions analyses (i.e. absence or presence of Fagus). Furthermore The lithology and sedimentological composition of a specific both clay members (the Belfeld Clay and the Tegelen Clay) lithostratigraphical unit depends on the depositional Sterksel Formation Sterksel Formation Sterksel Formation Sterksel Formation are defined in the same fluvial sequence on the Peel Block conditions and geomorphological setting (high-low energy,
Middle Pleistocene near Tegelen (chapter 3, 4) and extrapolation of this 15-25 m position in the floodplain). Its petrographical composition thick sequence to the up to 90 m thick stacked Rhine-Meuse reflects the provenance. The stratigraphical position deposits in the RVG (Zagwijn, 1963a) is very problematic. forms another major criterion for the definition of a The thin fluvial sequences near Tegelen probably reflect only lithostratigraphic unit. In case of the Upper Pliocene and Stramproy Formation Stramproy Formation Stramproy Formation Stramproy Formation a minor time period of the depositional history as registered Lower Pleistocene fluvial record of the southern Netherlands, in the RVG. Moreover the deposits all exhibit comparable the three criteria (lithology, stratigraphical position and lithological, petrographical, and depositional conditions. provenance) enable a subdivision of the fluvial deposits into
Pleistocene So, it is hard to determine which sedimentary cycle in the three formations, i.e. Kieseloolite Formation, Waalre Formation P l e i s t o c ne P RVG corresponds to the Tegelen area. and Stramproy Formation.
Peize 2.6.3 Stramproy Formation In the revised lithostratigraphical scheme, the Kieseloolite WA-3 WA-3 Formation The quartz-rich and stable heavy-minerals dominated Formation remains for its larger part unaltered. Compared to Lower Pleistocene Lower Waalre Formation deposits of the Stramproy Formation can be traced over the former definitions, the authors now exclude the uppermost Maassluis Maassluis Formation whole study area. So far, no further subdivision into members part of this unit because of its unstable heavy-mineral content Tegelen Member Fm. has been made. This is mainly because of gradual lateral which indicates that it is part of an Alpine connected Rhine
WA-2 WA-2 WA-2 changes in lithology and the absence of distinct marker system. These deposits now form the lowermost part of horizons. However, in spite of the absence of intra-formation the Waalre Formation (WA-1) and have been mapped in the boundaries, it seems possible to make a three fold subdivision subsurface of the RVG (Figs. 2.6, 2.8, 2.9, 2.11, 2.12). They based on the lithological composition (mainly grain-size also form the equivalent of the Oebel Beds in Germany. The Waalre Fm WA-1 Waalre Fm WA-1 Waalre Fm WA-1 distribution): Pliocene terrace deposits of the so-called East Meuse which Reuver Bed Reuver Bed Reuver Bed Oosterhout Oosterhout Formation • in the southern part of the RVG the up to nearly 100 m show a pure Meuse origin, are now no longer included in Kieseloolite Kieseloolite Kieseloolite Formation thick sequence of the Stramproy Formation is dominated the Kieseloolite Formation but form part of a separate unit
Pliocene Upper Pliocene Formation Formation Formation by sandy deposits and relatively thin clay layers and peat (Beegden Formation) describing all Plio-Pleistocene Meuse horizons (Figs. 2.7, 2.8, 2.9) . deposits. Legend • in the northern part of the RVG, the formation shows Erosion / non-deposition well-expressed fining-upward cycles with thick clay The revision of the Tertiary and Quaternary lithostratigraphy deposits in the upper part. These cycles always overlie of the Netherlands has revealed two new units describing the
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Early Pleistocene tidal and fluvial environments Reid, Cl. & Reid, E.M., 1915. The Pliocene Floras of the Dutch- Gebieten 1932-1937. Geologische Rundschau 29 (3/5): 223- in the southern Netherlands and northern Belgium, Dissertatie Prussian border. Mededelingen Rijksopsporingsdienst voor 273. Amsterdam: 1-190. Delfstoffen 6: 1-178. Felder, W.M. & Bosch, P.B., 1989. Geologische kaart van Zuid- Kasse, C. & Bohncke, S., 2001. Early Pleistocene fluvial Salvador, A. 1994. International Stratigraphic Guide. A guide to Limburg en omgeving, schaal 1:50.000. Afzettingen van de and estuarine records of climate change in the southern stratigraphic classification, terminology, and procedure, Second Maas. Rijks Geologische Dienst, Heerlen. Netherlands and northern Belgium. In: Maddy, D., Macklin, edition. Geological Society of America. 1-214.
40 41 Schäfer, A., Utescher, T., Klett, M. & Valdivia-Manchego, Westerhoff. W.E., Kemna, H.A. & Boenigk, W., 2008. The 3 The Lower Pleistocene fluvial (clay) deposits in the Maalbeek pit near M., 2005. The Cenozoic Lower Rhine Basin – rifting, confluence area of Rhine, Meuse, and Belgian rivers: Late Tegelen, The Netherlands sedimentation, and cyclic stratigraphy. International Journal Pliocene and Early Pleistocene fluvial history of the northern Earth Science (Geol. Rundsch.) 94. 621–639. Lower Rhine Embayment. Netherlands Journal of Geosciences/ Schreuder, A., 1943. Fossil Voles and other mammals (Desmana Geologie en Mijnbouw 87: 107-126. W. E. Westerhoff, P. Cleveringa, T. Meijer, Th. Van Kolfschoten & W.H. Zagwijn Talpa, Equus etc.) out of well-borings in the Netherlands. Wunstorf, W & Fliegel, G., 1910. Die Geologie des Verhandelingen Geologisch en Mijnbouwkundig Genootschap niederrheinischen Tieflandes. Abhandlungen Preußische Published as: Westerhoff, W.E., Cleveringa, P., Meijer, T., Kolfschoten, T. van & W.H. Zagwijn, 1998. The lower Pleistocene 13: 399-434. Geologische Landesanstalt N.F. 67: 1-172. fluvial (clay) deposits in the Maalbeek pit near Tegelen, the Netherlands. Mededelingen Nederlands Instituut voor Toegepaste Schreuder, A., 1950. De zoogdieren van de Klei van Tegelen. Zagwijn, W.H., 1957. Vegetation, climate and time-correlations Geowetenschappen TNO 60: 35-70. Geologie en Mijnbouw N.S. 12: 88. in the early Pleistocene of Europe. Geologie en Mijnbouw 19: Tavernier, R. & De Moor, G., 1974. L’évolution du basin de 233-244. Compared to the original paper published in 1998 the here presented version is adapted to the lithostratigraphical terminology l’Escaut. In: P.Macar (ed.) L’évolution Quaternaire des basins Zagwijn, W.H., 1960. Aspects of the Pliocene and Early as applied in this study. fluviaux de la Mer du Nord méridionale. Soc. Géol. de Pleistocene vegetation in the Netherlands. Mededelingen Belgique, Liège, 159-231 Geologische Stichting C-III-1 (5): 1-78. Abstract Tesch, P., 1908. Der niederländische Boden und die Ablagerungen Zagwijn, W.H., 1963a. Pollen-analytical investigations in the Tiglian Detailed studies of recently exposed Lower Pleistocene clay deposits and their fossil content (pollen, plant macrofossils, molluscs and des Rheines und der Maas aus der jüngeren Tertiär- und der of The Netherlands. Mededelingen Geologische Stichting 16: mammals) in the Maalbeek pit near Tegelen are presented. Two main sedimentary units are distinguished within the exposed clays. älteren Diluvialzeit. – Thesis Delft; Mitteilungen der Staatlichen 49-72. The lower one is interpreted as a flood-basin clay initially formed in a large stagnant waterbody with peat growth. The second clay unit Bohrverwaltung in den Niederlanden 1: 1-74. Zagwijn, W.H., 1963b. Pleistocene stratigraphy in the Netherlands, is deposited in an abandoned channel which was incised into the lower situated flood-basin clay and consists of a typical laminated clay. Tesch, P., 1911. Over Pleistoceen en Plioceen in den based on changes in vegetation and climate. Verhandelingen Based on the high amount of pollen from Fagus the lower part of the flood-basin clay is assigned to pollen zone T-A. The overlying part Nederlandschen bodem (II). Tijdschrift Aardrijkskundig Koninklijk Nederlands Geologisch en Mijnbouwkundig of the flood-basin clay is characterised by a pollen assemblage dominated by Ericaceae and Artemisia indicating a less dense vegetation Genootschap XXVIII(4): 628-647. Genootschap. Geologische serie, 21-2: 173-196. cover and/or cooler climatological circumstances. It represents the pollen zone T-B. The uppermost part of the flood-basin clay and Tesch, P., 1928. De stratigrafische grens Plioceen-Pleistoceen Zagwijn, W.H., 1974. Bemerkungen zur stratigraphischen the overlying laminated channel fill in Europa. Verslagen Geologische Sectie, Geologisch en Gliederung der plio-pleistozänen Schichten des are characterised by pollen assemblages that represent the early part of the pollen zone T-C. The molluscan, mammalian and Mijnbouwkundig Genootschap Nederland en Koloniën 1928, niederländischen-deutschen Grenzgebietes zwischen Venlo und palaeobotanical data all point to these conclusions. III: 203-211. Brüggen. Zeitschrift de Deutschen Geologisches Gesellschaft The earlier ascribed Eburonian age for the clay dominated by Ericaceae and Artemisia in the Maalbeek pit can now be rejected. Tesch, P., 1934. De opeenvolging van de Oud-Plistocene lagen in 125: 11-16. This adjustment of the Early Pleistocene stratigraphy in the Maalbeek pit corresponds better with the generally-accepted mammalian Nederland. Tijdschrift Aardrijkskundig Genootschap LI: 649- Zagwijn, W.H., 1982. Het begin van het IJstijdvak. Koninklijke stratigraphy in Europe. 675. Nederlandse Akademie van Wetenschappen, Verslag Afdeeling Tesch, P., 1937. Het voetstuk van Nederland. Tijdschrift Natuurkunde 91 (7): 54-59. Aardrijkskundig Genootschap LIV: 7-16. Zagwijn, W.H. & Zonneveld, J.I.S., 1956. The interglacial of 3.1 Introduction The larger part of the Lower Pleistocene clay in the Vandenberghe, J. & De Smet, P., 1979. Palaeomorphology in the Westerhoven. Geologie en Mijnbouw 18: 37-46. The excavation of Lower Pleistocene clay at Maalbeek neighbourhood of Tegelen is characterised by pollen eastern Scheldt basin (Central Belgium) –The Dijle-Demer- Zonneveld, J.I.S., 1947a. De grens Plio-Pleistoceen in Z.O. (Fig. 3.1, SE of Tegelen) has drawn attention of geologists assemblages of pollen zone T-C. Lithostratigraphically, these Grote Nete confluence area. Catena 6, 73-105. Nederland. Geologie en Mijnbouw N.S. 9: 180-190. since the beginning of the 20th century. During the early part clays are assigned to the Tegelen Clay (Zagwijn, 1963). As Van den Berg, M.W., 1996. Fluvial sequences of the Maas: a 10 Zonneveld, J.I.S., 1947b. Het Kwartair van het peelgebied en of the century it was thought that all clay deposits in this pit already mentioned, deposits belonging to the pollen zone T-A Ma record of neotectonics and climatic change at various time- de naaste omgeving. Een sedimentpetrologische studie. could be ascribed to the Tegelen Clay. The first introduction of have been reported until now from a site south of Maalbeek, scales. Thesis. Landbouwuniversiteit Wageningen: 1-181. Mededelingen van de Geologische Stichting, Serie C-VI-3: the Tegelen Clay in a lithostratigraphical sense was made by known in the literature as the Janssen-Dings pit (Van der Vlerk Van der Vlerk, I.M. & Florschütz, F., 1953. The palaeontological 1-233. Eugene Dubois (1905) followed by Reid and Reid (1915) who & Florschütz, 1953; Zagwijn, 1960, 1963; Boenigk, 1970). The base of the subdivision of the Pleistocene in the Netherlands. Zonneveld, J.I.S., 1950. De zware-mineralen-analyse en de introduced the stage name Teglian (=Tiglian). Several authors clay from this pit has been termed lithostratigraphically the Verhandelingen Koninklijke Akademie van Wetenschappen, Nederlandse prae-Riss-stratigrafie. Geologie en Mijnbouw 12: (e.g. Van der Vlerk & Florschütz, 1953; Zagwijn, 1960, 1963) Belfeld Clay (Zagwijn, 1963). It is stratigraphically below the Afdeling Natuurkunde, 1e Reeks XX (2): 1-58. 32-37. showed the complexity of the Early Pleistocene stratigraphy. Tegelen Clay. Van Regteren Altena, C.O., 1955. The Mollusca from the Zonneveld, J.I.S, 1958. Litho-stratigrafische eenheden in het Nowadays, all fluvial deposits supplied by the Rhine and The Maalbeek site is well-known because of finds of molars of Reuver Clay (Pliocene, Dutch-German border). Mededelingen Nederlandse Pleistoceen. Mededelingen van de Geologische Meuse in the Early Pleistocene are assigned to the Waalre Tapirus arvernensis and Anancus arvernensis (Kortenbout van Geologische Stichting N.S. 8: 87-93. Stichting N.S. 12: 31-64. Formation. Deposition took place during the Pretiglian and der Sluys, 1960; Zagwijn, 1963). Pollen analytical studies of Walsh, S.L., 2005. The role of stratotypes in stratigraphy. Part 1. Zonneveld, J.I.S., 1974. The terraces of the Maas (and the Tiglian Stages. clay layers in the pit were carried out by Zagwijn (1963) and Stratotype functions. Earth-Science Reviews 69: 307–332. Rhine) downstream of Maastricht. In: P.Macar (ed.) L’évolution The tripartition of the Tiglian into Tiglian A, B and C is based Urban (1978). Nota (1956) and Boenigk (1970) published heavy- Weerts, H.J.T., Cleveringa, P., Ebbing, J.H.J., De Lang, F.D. & Quaternaire des basins fluviaux de la Mer du Nord méridionale. on pollen analytical studies of clay layers within the Waalre mineral diagrams from sections exposed in the Maalbeek pit. Westerhoff, W.E., 2000. De lithostratigrafische indeling van Soc. Géol. de Belgique, Liège, 133-157. Formation (formerly Tegelen Formation; Zagwijn, 1963, 1992). All authors conclude that the clays are of Early Pleistocene Nederland Formaties uit het Tertiair en Kwartair. TNO Rapport The lower pollen zone, T-A, is pollen analytically characterised age. However, there is confusion about the precise position NITG 00-95-A. NITG-TNO, Utrecht. by high percentages of Fagus and is defined in the clay from in the stratigraphy (Boenigk, 1970; Zagwijn, 1974; Van Weerts, H.J.T. & Westerhoff, W.E., 2006. Lithostratigraphy (vol. the Janssen-Dings pit near Belfeld on German territory just Kolfschoten & Van der Meulen, 1986). 4, 2826-2840). In: S.A. Elias, Encyclopedia of Quaternary south of Maalbeek (Van der Vlerk & Florschütz, 1953; Zagwijn, The mammal remains from Maalbeek have been significant Science, four-volume set (Volume 1-4). Elsevier. 1963). The pollen and plant macrofossils found in this clay, for a long time in the debate on the stratigraphic position of Westerhoff, W.E. 2004. Upper Pliocene and Lower Pleistocene lithostratigraphically assigned as Belfeld Clay, indicate a the deposits. They all suggest an Early Pleistocene age older Rhine-Meuse deposits in the Tegelen-Reuver Area. With warm temperate climate. The Tiglian B, the following cooler than the Tiglian fauna from Russel-Tiglia (Schreuder, 1950a, contributions by H.A. Kemna. DEUQUA meeting 2004, phase, has been hitherto only pollen analytically described 1950b; Kortenbout van der Sluys, 1960; Van Kolfschoten & Nijmegen. Excursion guide: 79-130. in the fluvial sequences of the Roer Valley Graben (Zagwijn, Van der Meulen, 1986). However, this suggestion is Westerhoff, W.E., Wong, T.E. & Geluk, M.C., 2003. De opbouw 1963). The pollen zone T-C is mainly characterised by a warm inconsistent with the pollen analytical evidence from a clay van de ondergrond. In: De Mulder E.F.J., Geluk, M.C., Ritsema, temperate climate with several climatic changes (pollen layer in the Maalbeek pit, as published by Zagwijn (1963). I., Westerhoff ,W.E. & Wong, T.E. (eds). De ondergrond diagram Tegelen, Russel-Tiglia-Egypte pit; Zagwijn, 1963). Based on pollen studies of several deposits of Tiglian age and van Nederland. Nederlands Instituut voor Toegepaste assuming that the clay bed exposed at Maalbeek belongs Geowetenschappen TNO. Geologie van Nederland 7, 247-352. to the Tegelen Clay Member, Zagwijn (1963) concluded that
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