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Sedimentary Geology, 27 (1980) 1--81 1 © Elsevier Scientific Publishing Company, Amsterdam -- Printed in the Netherlands

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Sedimentary Geology, 27 (1980) 1--81 1 © Elsevier Scientific Publishing Company, Amsterdam -- Printed in the Netherlands Sedimentary Geology, 27 (1980) 1--81 1 © Elsevier Scientific Publishing Company, Amsterdam -- Printed in The Netherlands PRE-PERMIAN DEPOSITIONAL ENVIRONMENTS AROUND THE BRABANT MASSIF IN BELGIUM, THE NETHERLANDS AND GERMANY M.J.M. BLESS I J. BOUCKAERT 2, R CONIL 3, E. GROEBSENS 2 W. KASIG 4 E. PAPROTH 5, E. POTY 6, M. VAN STEENWINKEL 7, M. STREEL 8 and R. WALTER4 I Geological Bureau, Netherlands Geological Survey, Heerlen (the Netherlands) 2Geological Survey of Belgium, Brussels (Belgium) 3Lab. Paleontology, University of Louvain, Louvain-la-Neuve (Belgium) 4RWTH Aachen, Aachen (F.R. Germany) 5Geological Survey Nerthrhine-Westphalia, Krefeld (F.R. Germany) 6Lab. Paleozoology, University of Liege, Liege (Belgium) 7Lab. Paleontology, University of Leuven, Leuvan (Belgium) 8 Lab. Paleobotany and Palynology, University of Liege, Liege (Belgium) (Received 15 March 1980) ABSTRACT Bless, M.J.M., Bouckaert, J., Conil, R., Grsessens, E., Kasig, W., Paproth, E., Poty, E., Steenwinkel, M. van, Streel, M. and Walter, R., 1980. Pre-Permian depositianal environments around the Brabant Massif in Belgium, the Netherlands and Germany. Sediment. Geol.,27:1--81. Pre-Permian sedimentation in northwestern Europe has been controlled by the structural evolution of this area. Cambro-Silurian deposition has been influenced by partly synsedimentary movements (among others Ordovician- Silurian uplift south of the Brabant/Condroz zone, such as the £tavelot-Venn Massif). Presence, respectively absence of important late Caledonian deformation has subdivided northwestern Europe into three major sedimentary environments during the Devono-~arbonifarous: the Caledonian fold belt and the Cornwall- Rhenish Basin which are separated by the Belgo-Dutch platform. Subsequently, the Hercynian or Variscan orogenies have gradually reduced the sedimentary area end produced the overall withdrawal of the marine environment. Eventually, large-scale overthrusts - such as the Dinant Nappe - masked parts of the original sedimentary basins. INTRODUCTION Our knowledge about the Pre-Permian deposits around the Brabant Massif in Belgium, the Netherlands and Germany (Fig. I) varies from rather good for the Paleozoic outcrops in the Ardennes and the Rhenish Massif to very incomplete for the areas to the north where only few boreholes have penetrated the rocks below the coal-bearing Upper Carboniferous. The investigations on the Pre-Psrmian in the subsurface south of the Brabant Massif during the pa~ ten to fifteen years have increased our kn~w- ledge about the southward extension of the Midi Overthrust, the allochLhonous nature of the Dinant Synclinorium (here called Dinant Nappe),as well as Lh~ sediments below this Dinant Nappe. But they have also created many new problems because the facts observed during these studies did not fit into the old concepts hitherto accepted as classic. Also, the first published results of the exploration of the Pre-Permian ~n the North Sea have in part b~en quite surprising and force the geologist ~m develop new working hypotheses about the structural and sedimantological evolution of that area. The present paper summarizes several conoepts which are based upon these new findings. It should be stressed, however, that many of +,++ ,,,,- LO • o°ale~ ° oo -,AI O - ::. ":'::';..:-:.-y:.":: D • ::. o @ D minim, I; 'l Fig. I. Location of the Brabant Massif and the Pre-Psrmian outcrops of the Ardennes and Rhenish Massif. these ideas do not pretend to be anything more than working models that need to be checked and revised by future exploration. Structural complication: Oinant Nappe The evolution of northwestern Europe during Pre-Permian times can only be understood if we restore the allochthonous deposits of the Dinant Nappe to their original position. The allochthonous nature of the sediments in the Dinant Synclinorium was already suggested by Fourmarier (1913), who believed the Namur Basin to extend south of Dinant below the Midi Overthrust. This is supported by several seismic surveys recently carried out in northern France (Clement, 1963), the Famenne area of southern Belgium (non-published reports of the Geological Survey of Belgium, 1976-1978; Bless et al., ~977a, b), and in the Stavelot-Venn Massif southeast of Aachen in the F.R.G. (Bartelsen & Meissner, 1979; M. & R. TeichmUller, 1979). These investigations prove a minimum extension of the Midi Overthrust of 175x40 km (Fig. 2). However, it seams reasonable to believe that this overthrust extends beyond the area studied thus far. Thrust-folded IBIock-fau ted autochthonous deposits allochthonous rocks I 6 cP Fig, 2. Cartoon showing the proven extension of the Dinant Nappe, (From Bless et al., Ig8Ob.) The hypotheses, that the overthrust does not extend across the metamorphic Ardennan Belt (Bless et al., 1977a, b; R. & M. TeichmUller, 1979) seems alrea dy out of date since the thrust plane has been traced below the Stavelot-Venn Massif (Barteleen & Meieener, 1979). It appears more acceptable to suppose nowadays that the whole Dinant Nappa was derived from the northern flanks of the Armorican-Mid German Highs. This might imply that the Cambro-Silurian rocks of the Ardannee and Btavelot-Venn Massif and most of the Lower Devonian deposits in the Dinant Nappe once formed the western extension of, say, the Taunus-HunsrUck! This hypothesis also implies that the eastern border of the Dinant Nappe might coincide more or less with the N-S trending Eifel Zone. It is worthwhile to compare the N-S trending Eifel Zone and the N-S trenoing Ems Low, occurring farther north, which may be remnants of the same old 3inea merit. Little can be said about the western extension of the nappe structure, since this is covered by a thick sequence of Mesozoic strata. If we can only speculate about the real extension of the overthrust plane, we should say less about the possible displacement along the same. One may imagine that large parts of the Dinant Nappe rest directly upon Cambro- Silurian or even Precambrian basement. But, on the other hand, it cannot be excluded without further study that Devono-Carboniferous deposits reach fez to the south below the overthrust as might be deduced from thick - partly coal-bearing - Silesian strata in the autochthonous sequence of the Jeumont Borehole in northern France, as well as from the hypothetical extension o5 Devono-Dinantian avaporite deposits (recognized in several boreholes: Annappes-1, Leuze, Tournai and St.-Ghislain) below the Famenne and Ourbuy region (Bouckaert st al., 1977; Bless et el., 1977b, 1980a). Stratigraphical complication: reworked microfoseils Exact knowledge of the age of sediments is indispensable for the con- struction of reliable paleogeographic maps. Frequently, the age is deter- mined by means of microfossils. Often, microfossils are only considered as useful stratigraphic tools. From that viewpoint, the occurrence of reworked specimens (derived from stratigraphically older deposits) in a microfossil assemblage may be considered as a 'contamination' that may complicate the age determination. However, such reworked microfossils can also be regaroed as a special kind of 'accessory mineral grains' in the sediment. In that case, they may help in tracing the origin of (part of) the sediment, in ~ similar way as - for instance - heavy mineral associations. The most commonly occurring reworked microfossils are palynomorphs. The ages of sediments containing reworked palynomorphs are not distributed random~ ly on the geological time scale (Fig. 3). Distinct peaks occur in the Quater- nary, Lower Tertiary, Neoeomian, Rhaet/Dogger, Westphalian, Upper Devonian/ Dinantian and Lower Devonian. The fact that these peaks become smaller - ano therefore perhaps less convincing at first sight - is easily explained if we consider the circumstance that the number of papers dealing with palyno~ morphe is much lower for older than for younger deposits. We do not believe that this curious distribution of the reworked palyno-- morph record is due to a haphazard literature compilation. It rather suggests that there were periods in geological history during which the reworking pro- case was intensified by geological phenomena. We presume that a correlation Geological Time Table Main orogenic events Quaternary Holocene IIIIIIIIIIlUlIIIIIIIIII~ [Changes of base level) Pleistocene Illllllllllll"lllllllllll/ ( Olaciahons ) Pliocene Miocene I Tertiary Oligocene Iiiin Eocene IIIIIIIIIIII '~ Paleocene IIiiiiiiiiiiii/ Loramian/ Senonian I II / 'Subhercyn ian Turonian IIII Cenomanian Cretaceous Albian IiiiiI Aptian III Barremian III Neocomian (incI.Wealden) I Late Kimmerian Maim Jurassic Dogger Lias Rhaet Early Kirnmerian Keuper Triassic Muschelkalk Buntsandstein Thuringian Permian Saxonian Autunian Stephanian Westphalian Asturian Carboniferous Narnurian I Dinantian IIII11) Upper III / Bretonian Devonian Middle Lower I, ) Ludlovian/Pridolian Late Caledonian Silurian Wenlockian Llandoverian Ordovician Cambrian Fig. 3. Tentative correlation between recorded ages of deposits containing reworked palynomorphs and main orogenic events, as well as glaciations and sea level changes in the Quaternary. (From Streel & Bless, Ig80.) can be made between these peaks and the main orogenic events inasmuch as Tertiary and older deposits are concerned, and with glaciations and base level changes (sea level changes) during the Ouaternary. Important reworked palynomorphs assemblages in the Pre-Permian deposits around the Brabant Massif have been described from the Silurian, Lower Devonian and Upper Weatphalian
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