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PDF Viewing Archiving 300 Mémoires pour servir à l'Explication Toelichtende Verhandelingen des Cartes Géologiques et Minières voorde Geologische en Mijnkaarten de la Belgique van België Mémoire No 21 Verhandeling N° 21 Subsurface structural analysis of the late-Dinantian carbonate shelf at the northern flank of the Brabant Massif (Campine Basin, N-Belgium). by R. DREESEN, J. BOUCKAERT, M. DUSAR, J. SOl LLE & N. VANDENBERGHE MINISTERE DES AFFAIRES ECONOMIQUES MINISTERIE VAN ECONOMISCHE ZAKEN ADMINISTRATION DES MINES BESTUUR VAN HET MIJNWEZEN Service Géologique de Belgique Belgische Geologische Dienst 13, rue Jenner 13,Jennerstr.aat 1040 BRUXELLES 1040 BRUSSEL Mé~. Expl. Cartes Géologiques et Minières de la Belgique 1987 N° 21 37p. 18 fig. Toelicht. Verhand. Geologische en Mijnkaarten van België blz. tabl. SUBSURFACE STRUCTURAL ANAL VSIS OF THE LATE-DINANTIAN CARBONATE SHELF AT THE NORTHERN FLANK OF THE BRABANT MASSIF (CAMPINE BASIN, N-BELGIUM). 1. INTRODUCTION 1.1. Seismic surveys in the Antwerp Campine area 1.2. Geological - stratigraph ical setting 1.3. Main results 2. THE DINANTIAN CARBONATE SUBCROP 2. 1. Sei smic character 2.2. General trends and anomalies 2.2.1. Western zone 2.2.2. Eastern zone 2.2.3. Transition zone 2.3. Deformations 2.3.1. Growth fault 2.3.2. Collapse structures 2.3.3. T ectonics 2.3.3.1. Graben faults 2.3.3.2. Central belt 2.4. 1nternal and underlying structures 2.4.1. 1nternal structures 2.4.2. Underlying deep reflectors 3. RELATIONSHIP WITH OVERLYING STRATA 3.1. Upper Carboniferous 3.1.1. Namurian 3.1.2. Westphalian 3.2. Mesozoicum 3.3. Cenozoicum 4. GEOLOGICWORKING MODEL 4.1. Paleogeography 4.2. Structural evolution 4.3. Collapse structures and sinkholes 5. REFERENCES ENCLOSURES 1. Location map seismic profiles ( 1974-1982) and cross-sections A to G .Il. lsochron map of the top of the Dinantian Ill. 1sochron map of the base of the Cretaceous IV. Cross-sections A to G TABLES -3- SUBSURFACE STRUCTURAL ANAL YSIS OF THE LATE-DINANTIAN CARBONATE SHELF AT THE NORTHERN FLANK OF THE BRABAN"'F MASSIF (CAMPINE BASIN, N-BELGIUM). by 1 2 2 3 4 R. DREESEN , J. BOUCKAERT , M. DUSAR , J. SOILLE & N. VANDENBERGHE INTRODUCTION haut boreholes are the best documented (BLESS et al., 1976; 1981) (fig. 2). 1.1.- SEl SMIC SURVEYS IN THE ANTWERP The Heibaart- Loenhout borehole (He 1 and CAMPINE~AREA 1 bis) has been drilled in 1962 by PETROFINA. Coring was discontinuous. Lower Namurian strata underlying 1n table A (p. 36) a list is given of ali the seismic the basal Cretaceous unconformity were reached at surveys carried out in the a rea investigated. 1n particular 1052 m and the Dinantian at 1138 m. The Upper the recent campaigns 4, 5, 6 and more especially 7 were Devonian sandstones and marine shales sequence was usèd in our study. reached at 1461 m. The borehole penetrated the Si­ The different acquisition and processing para­ lurian subcrop at 1627 m. Between 1977 and 1980 meters of the reë\lnt dmp"àigns are listed in table B severa! boreholes (OZ H 1 - OZ H6) were drilled on (p.37). The weil seismic velocity surveys available are top of the Heibaart structure on behalf of DISTRIGAZ, indicated in table C (p. 37). in arder to test the possible reservoir qualities of the uppermost karstic zone in the Dinantian carbonates for subsurface gas storage. For a detailed description 1.2.- GEOLOGICAL - STRATIGRAPHICAL SETTING of the cored intervals of these boreholes (microfacies - microfauna - depositional environments) the reader is The studied area represents the southernmost part · referred to BLESS et al. (1981). The cored intervals of the Campine- Brabant Basin at the northeastern located at the top of the karstified llinantian limestone edge of the London- Brabant Màssif (fig. 1). The geolo­ have been attributed to the basal Warnantlan (V3b). gical framework of the area is made up of a sequence of Microfacies analysis of the cores of qoreholes OZ H2 slightly north-dipping Cenozoic and Mesozoic strata, and OZ H4 (S-flank of the Heibaart dame) pointed which unconformably overly steeper but also north­ out a deposition in an open marine shelf lagoon under dipping Devono- Carboniferous strata, which in their shallow water conditions, whereas the cores of the other <:urn cover a structurally more complex Cambro -Silu­ boreholes (ali located on the N-flank) indicated deposi­ rian basement (LEGRAND, 1968).· tion on tidal flats in very shallow lagoons with restricted water circulation and hypersaline waters. The Turnhout The Cenozoic deposits reach a thickness of about borehole (drilled between 1953 and 1955 for the Ins­ 600 m and comprise the following lithostratigraphical titut National de 1'1 ndustrie Charbonnière and the Belgian suite (from top to bottom) : Pleistocene Campine clays Geological Survey) reached the Upper Carboniferous and sands, the Neogene glauconitic Sands, the Boom at 1002 m and the top of the Dinantian at 2162 m. Clay, the Kallo Clays and fine Sands complex, the Lithological descriptions, especially of the Silesian, Lede-Brussel - Panisel Sands, the 1eper Clay and the have been published by DELMER ( 1962, 1963). The Landen- Heers Clays and Maris. reader is referred to BLESS et al. ( 1976) for a review The Mesozoic is essentially composed of Upper­ Cretaceous (Campanian- Maestrichtian) chalky lime­ stone and mari deposits (about 200 m thick). Present,ly at N{EB, Liège. The Paleozoic (Pre-Permian) subcrop h~s· been . 2 Billgian Geological Survey, Brussels. reached by severa! drillholes in the Campine area, 3 Distrigaz, N.V.- Brussels. East of Antwerpen, of which the Heibaart and Turn- 4 Presently at K.U. Leuven. -4- 0 50 Km r.:-:-:1 l:..:...:..:..: Q - Dinantian r::::::::l c § ll1lTllflllT11l U p p e r . l.;_;_;_;_;_;_; ll.ll.I1Wlli.ll M i d d l e 0 evo n 1an ~ Aegir marker band--- ~ --'-'-'-'--"'-'"--'--'"------------- ~ 8 ....... Lower Devonian Catharina marker band-A- ~ ~ Cambro- Silurien ~Sarnsbank marker band 3: ~Narhurian- -Pre- Cambrian ++#.f-.1. Belgian Dutch Boundary u Location of mapped subsurface from Van Staalduinen et al. (1979) The Geology of the Netherlands Figure 1. - General geological situation map. - 5- ~NHOUT TURNHOUT KESSEL BOOIS::HOT RILLAAR LOKSBERGEN HALEN Na -581 V3c 1 1 V3a-b 1 1 ----- - 753 Lower ? Warnantian \ 1 -.810 Upper V3b W:lrnantian Cf Go!' Lower Warnant ion V2b­ Livi an .... V3a ___ __ _ ---'"-=~-iz=CIOI- 937 ---- V2a? 563 -1429 ------ - 957 -299 Motiniacian -592 -311 Dev? -612 V2a . D-376 .. · .. -695 -555 Via -587 -1604 - 2407 Sil -619 VJ? V1a -684 ? -2508 NEDERLAND -2589 ? -1339 Figure 2.- Stratigraphie correlation of the Dinantian weil sections in the Campine area. - 6- of the microfaunal content and biostratigraphic con­ The Dinantian- Namurian unconformity might have clusions on the D inantian. M icrofaunal assemblages acted as a flat-lying sliding plane for the displacement (Foraminifera) indicated an V1a through V3c (Moli­ and the stretching of the Namurian strata. This growth niacian - Warnacian) age for the penetrated carbonates. fault may represent the northernmost limit of the None of the boreholes in the studied area has yielded shallow Dinantian carbonate shelf : farther to the a stratigraphically continuous sequence .of Dinantian North, Kulm-type Dinantian deposits might explain rocks thus far. the disappearance of the outspoken Dinantian lime­ From the frequent occurrence of stratigraphie gaps, stone reflector. unconformities, hardgrounds, breccias and reworked The preserved thickness of the Westphalian does microfossil assemblages in the studied boreholes N of not exceed 575 rn in the Turnhout borehole (DELMER, the Brabant Massif, it is clear that severa! epeirogenic 1962) whereas it is completely lacking on top of the movements have influenced the sedimentation pattern Heibaart structure. Obviously these thickness figures during late Dinantian times (BLESS et al. 1976, 1981). are determined by the structural dip of the Upper Continental facies have even been recorded from the Carboniferous and the post-Westphalian to pre-Upper Booischot borehole : conglomerates, sandstones, corn­ Cretaceous erosion. stones, paleosoils, ali dated V2a (LEGRAND, 1964; An overlap-sequence on top of one of the more BLESSetal., 1976). continuous sandstone reflectors might indicate a Na­ The Namurian is incomplete in the Campine Basin murian-Westphalian unconformable contact (VAN­ since the Pendleian and basal Arnsbergian strata are DENBERGHE, 1982). missing (BOUCKAERT, 1967). This stratigraphie hiatus The major and also the youngest tectonic fea­ is the result of a widespread regression. coinciding with orogenie movements of the sudetic phase (GRAULICH, tures in the studied area finally are the NNW-SSE 1962). This regression affected essentially the near­ directed tensional faults which affect the Carboniferous strata as weil as the overlying Meso-Cenozoic deposits. shore and inner shelf areas of the southern borders of These important faults are related to the Roer Valley ·the Brabant- Campine Basin. Graben boundary faults of the Netherlands Central The subsequent transgression gradually spread out Basin. They have been active at !east since the late across the shoals but was only completed in Kinderscou­ Paleozoic. During most of the Meso-Ceriozoic they tian times (BOUCKAERT, 1967; BLESSetal., l980). have been reactivated, sometimes in opposite senses, The age of the oldest Namurian strata in the Turnhout resulting in thickness variations of severa! Cenozoic borehole is Upper Arnsbergian ( E2c) whereas the strati­ formations in the NE-part of B.elgi!Jm (VAN STAAL­ graphical gap between Dinantian and Namurian extends DUINEN et al., 1979). into the Kinderscoutian most probably, in the Heibaart boreholes(BLESSetal., 1980, 1981). Thickness variation along the northern border of the 1.3.- MAIN RESULTS Brabant Massif is relatively small (500 -680 rn over a distance of more th an 100 km). The compilation of subsurface structural data However the preserved thickness of the Namurian has from severa! reflection seismic surveys, carried out been reduced to Jess than 70 rn over the particular between 1974 and 1982, resulted in a series of struc­ Heibaart antiform structure due to post-Westphalian tural isochron maps covering a surface of about 400 km2 pre-Cretaceous erosion.
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