an attempt of time calibration of the Lower Tournaisian (Hastarian Substage) based on orbitally forced sequences

in Document de l'Institut Scientifique, Rabat (2013), 26

Sedimentology and magnetic susceptibility of Mississippian (Tournaisian) carbonate sections in Belgium

in Bulletin of Geosciences (2013), 88(1), 69-82

Magnetic susceptibility (MS) and biostratigraphy have been used to correlate better the reference sections of Belgian Tournaisian, the Rivage road and railway sections and the Gendron-Celles railway ... [more ▼]

Magnetic susceptibility (MS) and biostratigraphy have been used to correlate better the reference sections of Belgian Tournaisian, the Rivage road and railway sections and the Gendron-Celles railway section. These 200 m thick time-equivalent sections are about sixty kilometres apart and belong to two different sedimentation areas: a shallow ramp setting for Rivage (Condroz Sedimentation Area, Hance et al., 2001) and a subsiding area for Gendron (Dinant Sedimentation Area). The sedimentological model shows that both sections are characterized by a bioclastic dominated sedimentation (crinoids-peloids-algae assemblages), interrupted by more argillaceous facies related to rapid sea-level rises (crinoids-brachiopods-bryozoans assemblages). Accommodation was significantly higher in the DSA and allowed the development of Waulsortian buildups during the Ivorian. Variations of magnetic susceptibility (MS) seem to be related to fluctuations in detrital input and carbonate productivity. MS evolution with palaeogeography can be integrated in the Da Silva et al. (2009a) model for the Devonian ramp system: external ramp settings have low carbonate productivity, low water agitation and high MS, whereas more proximal environments are characterized by higher carbonate productivity, higher water agitation and lower MS. Carbonate buildups show the lowest MS and highest productivity. MS curves are in agreement with the 3rd-order sequential interpretation. Lowstand system tracts (LST) show the highest MS values while transgressive system tracts (TST) are characterized by decreasing values and highstand system tracts/ falling stage system tracts (HST/FSST) by the lowest values. [less ▲]

Cours de géologie

Learning material (2012)

Notes du cours de géologie de 1 bac en géologie et de 2 bac en géographie

Paléontologie des Invertébrés - Notes de Travaux Pratiques

Learning material (2012)

Proceedings of the XIth International Symposium on Fossil Cnidaria and Porifera, Liège, Belgium, August 19-29, 2011: Preface

in Geologica Belgica (2012), 15(4), 200-203

Les géosites d'Ampsin et d'Engis (Belgique) : deux exemples de reconversion de carrières désaffectées

in Blieck, A.; Auguste, P.; Derycke, C. (Eds.) Programme et résumés (2011, October)

Interaction between eustacy and block-faulting in the Carboniferous of the Visé-Maastricht area (Belgium, the Netherlands)

in Zeitschrift der Deutschen Gesellschaft für Geowissenschaften [=ZDGG] (2011), 162(2), 117-126

The Visé–Maastricht sedimentation area (VSA) is situated at the eastern end of the Brabant Massif and suffered block-faulting tectonics during Lower Carboniferous time. The south edge of the VSA, the area ... [more ▼]

The Visé–Maastricht sedimentation area (VSA) is situated at the eastern end of the Brabant Massif and suffered block-faulting tectonics during Lower Carboniferous time. The south edge of the VSA, the area corresponding now to the vicinity of Visé, comprised three main tectonic blocks: the Hermalle-sous-Argenteau, Souvré and Bombaye blocks. They were bounded to south by the Booze–Val-Dieu block. To the north, in the vicinity of Maastricht, blocks are not well differ- entiated and are referred to as the Maastricht block system. From the end of the Tournaisian, the latter evolved into a rap- idly subsiding graben, recording mainly debris fl ows and limestone turbidites, whereas the southern blocks remained rela- tively high. Through much of Lower Carboniferous time, they were emergent, but during high eustatic sea levels, they were fl ooded and covered by limestone deposits. The differences in the nature and the age of the deposits between blocks result from the interaction between block-faulting and eustacy. In the VSA, the Upper Devonian and Lower Tournaisian (Hastarian) deposits are similar to those known in the north part of the Namur-Dinant Basin. But from the late Tournaisian (Ivorian), the uplift of the Booze–Val-Dieu block prevented all connections with the Namur-Dinant Basin and the VSA became linked with the Campine Basin. The Souvré block subsided from the latest Givetian to the late Frasnian and recorded a thick middle Frasnian limestone series, but was later emergent, so much that karstic cavities developed. The Souvré block was submerged for a short time at the top of the Tournaisian, during the very high highstand (HST) corresponding to eustatic sequence 4, and the caves fi lled up with sediments. The Hermalle-sous-Argenteau and the Bombaye blocks, situated respectively west and east of the Souvré block, evolved in the same way during the late Devonian. They subsided slightly from the earliest Tournaisian to the late Viséan (Warnan- tian), but usually remained emergent and recorded deposits only during times of high eustatic levels corresponding to the early Tournaisian (for the Bombaye block), the end of the Tournaisian (HST of sequence 4), the end of the early Viséan (HST of sequence 6), then the late Viséan (HST of sequences 9 and 10). In its southern part, the Hermalle-sous-Argenteau block recorded also lowermost Viséan limestones correlated with the highstand of the eustatic sequence 5, probably as a result of the tilting of the block to the south at this time. [less ▲]

11th Symposium on Fossil Cnidaria and Porifera, Liège, August 19-29, 2011: Abstracts

in Kölner Forum für Geologie und Paläontologie (2011), 19

The Belgian collections of fossil Cnidaria and Porifera

in Kölner Forum für Geologie und Paläontologie (2011), 19

Uppermost Devonian and Dinantian Rugose Corals from Southern Belgium and surrounding areas

in Kölner Forum für Geologie und Paläontologie (2011), 20