Middle Devonian to Dinantian Sedimentation in the Campine Basin (Northern Belgium): Its Relation to Variscan Tectonism

  1. L. E. Frostick4 and
  2. R. J. Steel5
  1. P. Muchez1,2 and
  2. V. Langenaeker3

Published Online: 16 APR 2009

DOI: 10.1002/9781444304053.ch10

Tectonic Controls and Signatures in Sedimentary Successions

Tectonic Controls and Signatures in Sedimentary Successions

How to Cite

Muchez, P. and Langenaeker, V. (1994) Middle Devonian to Dinantian Sedimentation in the Campine Basin (Northern Belgium): Its Relation to Variscan Tectonism, in Tectonic Controls and Signatures in Sedimentary Successions (eds L. E. Frostick and R. J. Steel), Blackwell Publishing Ltd., Oxford, UK. doi: 10.1002/9781444304053.ch10

Editor Information

  1. 4

    Reading, UK

  2. 5

    Bergen, Norway

Author Information

  1. 1

    Fysico-chemische geologie, K.U. Leuven, Celestijnenlaan 200C, B-3001 Heverlee, Belgium

  2. 2

    Senior research assistant National Fund for Scientific Research, Belgium

  3. 3

    Historische geologie, K.U. Leuven, Redingenstraat 16bis, B-3000 Leuven, Belgium

Publication History

  1. Published Online: 16 APR 2009
  2. Published Print: 28 FEB 1994

ISBN Information

Print ISBN: 9780632037452

Online ISBN: 9781444304053



  • middle Devonian to Dinantian sedimentation in Campine basin;
  • evolution of Campine basin during Devonian and Dinantian;
  • synsedimentary fault activity and large scale extensional tectonism;
  • extensional tectonism;
  • synsedimentary faults active in Campine Basin


The relationship between synsedimentary faulting and sedimentation has been investigated in the Devonian–Dinantian strata of the Campine Basin (northern Belgium). The basin was formed during the Middle Devonian and was enhanced by widespread extensional faulting in the Chadian/Early Arundian and in the Asbian. A phase of inversion occurred at the end of the Dinantian. The Devonian is characterized by the deposition of siliciclastic sediments in one or more half-graben structures. Facies patterns developed in a S–N direction, with Chadian/Early Arundian siliciclastic carbonates deposited near the Brabant–Wales Massif, and open marine, shallow subtidal limestones bordered to the north by cryptalgal boundstones. During the Asbian, microbial buildups developed on the shelf and at the shelf margin. An approximately E–W trending growth fault possibly formed the boundary between this shelf and the basinal environment. On the shelf, synsedimentary faults are oriented subparallel to the northern margin of the Brabant–Wales Massif and are generally NW–SE trending in the western part and E–W trending in the eastern part. The Brabant–Wales Massif appears to have exerted a major influence on the fault directions.

The S–N trending facies patterns, the c. E–W oriented growth fault and the E–W direction of the extensional faults in the eastern part of the Campine Basin are compatible with N–S extension, active during the Middle Devonian to Dinantian interval.

Major synsedimentary tectonism during the Visean was broadly synchronous in northern England, North Wales, Ireland (Dublin area) and northern Belgium. Basin initiation began later in Britain and Ireland (Late Devonian). According to Leeder (1982) the N–S extension, which was active north of the Brabant–Wales Massif during part of the Devonian and during the Dinantian, occurred as a result of back-arc stretching to the north of an active plate collision zone, situated in the South Brittany–Massif Central–Vosges area. Synsedimentary tectonism in the Campine Basin is synchronous with the onset of compressional phases in the Rhenohercynian Basin and the closure of this back-arc basin.