Elsevier

Tectonophysics

Volume 300, Issues 1–4, 31 December 1998, Pages 103-129
Tectonophysics

Mechanical controls on collision-related compressional intraplate deformation

https://doi.org/10.1016/S0040-1951(98)00236-4Get rights and content

Abstract

Intraplate compressional features, such as inverted extensional basins, upthrust basement blocks and whole lithospheric folds, play an important role in the structural framework of many cratons. Although compressional intraplate deformation can occur in a number of dynamic settings, stresses related to collisional plate coupling appear to be responsible for the development of the most important compressional intraplate structures. These can occur at distances of up to ±1600 km from a collision front, both in the fore-arc (foreland) and back-arc (hinterland) positions with respect to the subduction system controlling the evolution of the corresponding orogen. Back-arc compression associated with island arcs and Andean-type orogens occurs during periods of increased convergence rates between the subducting and overriding plates. For the build-up of intraplate compressional stresses in fore-arc and foreland domains, four collision-related scenarios are envisaged: (1) during the initiation of a subduction zone along a passive margin or within an oceanic basin; (2) during subduction impediment caused by the arrival of more buoyant crust, such as an oceanic plateau or a microcontinent at a subduction zone; (3) during the initial collision of an orogenic wedge with a passive margin, depending on the lithospheric and crustal configuration of the latter, the presence or absence of a thick passive margin sedimentary prism, and convergence rates and directions; (4) during post-collisional over-thickening and uplift of an orogenic wedge. The build-up of collision-related compressional intraplate stresses is indicative for mechanical coupling between an orogenic wedge and its fore- and/or hinterland. Crustal-scale intraplate deformation reflects mechanical coupling at crustal levels whereas lithosphere-scale deformation indicates mechanical coupling at the level of the mantle-lithosphere, probably in response to collisional lithospheric over-thickening of the orogen, slab detachment and the development of a mantle back-stop. The intensity of collisional coupling between an orogen and its fore- and hinterland is temporally and spatially variable. This can be a function of oblique collision. However, the build-up of high pore fluid pressures in subducted sediments may also account for mechanical decoupling of an orogen and its fore- and/or hinterland. Processes governing mechanical coupling/decoupling of orogens and fore- and hinterlands are still poorly understood and require further research. Localization of collision-related compressional intraplate deformations is controlled by spatial and temporal strength variations of the lithosphere in which the thermal regime, the crustal thickness, the pattern of pre-existing crustal and mantle discontinuities, as well as sedimentary loads and their thermal blanketing effect play an important role. The stratigraphic record of collision-related intraplate compressional deformation can contribute to dating of orogenic activity affecting the respective plate margin.

Introduction

Intraplate compressional structures range from uplift of broad arches and accelerated basin subsidence, involving whole lithospheric buckling, to crustal-scale folding and, by reactivation of pre-existing crustal discontinuities, to upthrusting of basement blocks and inversion of tensional hanging-wall basins. Intraplate compressional features play an important role in the structural framework of many cratons. Such structures can develop (1) in forelands of orogens in response to collisional mechanical coupling of the orogenic wedge with the foreland plate, (2) in back-arc areas during periods of increasing convergence rates between the colliding plates, (3) in oceanic basins where they may be considered as precursors to the development of new subduction zones, (4) along major wrench systems, (5) in multi-directional rift systems in response to stress re-orientation, (6) on passive margins, partly in the projection of intra-oceanic transform faults (Ziegler et al., 1995).

The World Stress Map demonstrates that horizontal compressional stresses can be transmitted over great distances through continental and oceanic lithosphere (Zoback, 1992). Although a number of dynamic processes contribute towards the build-up of intraplate compressional stresses, forces related to collisional plate coupling appear to be responsible for the most important compressional intraplate deformations. These can occur in hinterland as well as in foreland domains of orogenic wedges and at distances of up to ±1600 km from contemporaneous thrust fronts (Ziegler et al., 1995).

The stratigraphic record preserved in sedimentary basins permits to closely date the age of extensional as well as compressional intraplate deformation. Therefore, intraplate deformation plays a pre-eminent role in monitoring the timing of stress changes within continental cratons. As such, the stratigraphic record of collision-related compressional intraplate deformation can contribute towards the dating of orogenic activity affecting a respective plate margin.

The spatial and temporal development of compressional intraplate deformations is controlled by the interaction of fluctuating intraplate stresses and spatial and temporal strength changes of the lithosphere. The strength configuration of the lithosphere primarily depends on its thermo-mechanical structure that can change due to deformation of the lithosphere and its transient thermal equilibration. In many intraplate settings sedimentary basins are characterized by relatively steady state strengths prior to the onset of compressional intraplate deformation (van Wees and Stephenson, 1995; Ziegler et al., 1995). As the onset of compressional basin reactivation reflects a relative increase or a reorientation of the intraplate stress field, intraplate deformations are particularly sensitive recorders of the timing of stress fluctuations. On the other hand, given a relatively constant stress field, spatial variations in the onset of compressional intraplate deformation are controlled by the spatial strength distribution within the lithosphere. However, as the strength of the lithosphere increases during basin inversion, locking of earlier inverted basins can control the progressive propagation of far-field compressional deformations into the interior of continental cratons (Ziegler, 1987; van Wees et al., 1992; Ziegler et al., 1995).

In this paper we summarize the occurrence of collision-related intraplate compressional structures, explore the evolution of the continental mantle-lithosphere, analyze the effects of different modes of rifting and sediment loading on the rheological structure of the lithosphere, and discuss mechanical controls on the development of collision-related compressional intraplate structures in terms of orogenic processes affecting the respective plate margins. We realize that this paper assumes a considerable knowledge of global geology and that it would have been desirable to illustrate all examples discussed. However, this would have expanded this already long paper beyond acceptable limits. Therefore, we have endeavoured to provide the reader with a comprehensive reference list.

Section snippets

Occurrence of collision-related intraplate compressional deformations

Compressional and transpressional intraplate structures can occur at distances of up to 1600 km from a collisional margin, as indicated, for instance, by the Paleocene deformation of the northern Alpine foreland (Ziegler, 1990) and the latest Carboniferous–Early Permian development of the Ancestral Rocky Mountains in the foreland of the Appalachian–Ouachita–Marathon orogen (Ross and Ross, 1985, Ross and Ross, 1986; Kluth, 1986; Stevenson and Baars, 1986; Oldow et al., 1989; Ziegler, 1989).

Oceanic and continental lithosphere

In contrast to continental lithosphere, the lithosphere of the present oceanic basins is young and ranges in age from Middle Jurassic to Recent (Cande et al., 1989). Its crustal parts consist of MORB basalts, sheeted dykes and gabbros; lateral thickness and compositional variations depend on spreading rates, the presence or absence of ridge-centred plumes (N- and E-MORB) and intraplate hotspot activity. The mantle part of oceanic lithosphere is composed of asthenospheric material depleted in

Rifting of continental lithosphere

During rifting, culminating in the opening of new Atlantic-type oceanic basins, the continental lithosphere is stretched and the subcrustal mantle thermally attenuated, particularly in the presence of a mantle plume. Upon termination of rifting activity, or after crustal separation has been achieved and the respective passive margins have moved away from the seafloor spreading axis, the thermally destabilized continental lithosphere re-equilibrates with the asthenosphere (McKenzie, 1978;

Scenarios for fore-arc and foreland compressional deformation

We envisage four collision-related scenarios for the build-up of horizontal intraplate compressional stresses in fore-arc and foreland domains, namely: (1) during the initiation of subduction zones along passive margins or within oceanic basins; (2) during impediment of subduction processes caused by the arrival of a more buoyant crustal element, such as an oceanic plateau, transform ridge, arc or a microcontinent at a subduction zone; (3) during the initial collision of an orogenic wedge with

Mechanisms controlling mechanical coupling of orogenic wedges and forelands

The timing and intensity of intraplate compressional deformations indicate that mechanical coupling between an evolving orogen and its foreland can vary considerably. For instance, for the East Alpine–North Carpathian orogen, intense Senonian/Paleocene foreland deformations indicate strong mechanical coupling between the foreland and the orogenic wedge during their initial collision stage; however, during the Eocene–Early Miocene emplacement of nappes on the foreland, mechanical coupling

Conclusions

Collision-related compressional intraplate structures can be associated with Andean- and Himalayan-type orogens and can occur in back-arc as well as in fore-arc domains. Such deformation, ranging from crustal- to lithosphere-scales, can involve reactivation of pre-existing crustal discontinuities, resulting in the inversion of tensional hanging-wall basins and upthrusting of basement blocks, as well as whole lithospheric buckling, including uplift of broad arches and accelerated subsidence of

Acknowledgements

Wouter Brokx is thanked for his dedicated assistance in preparing the text figures for this paper. Thanks are extended to Alastair Robertson, François Roure, Gérard Stampfli, Jacques Touret and Marjorie Wilson for their constructive comments on an earlier version of this paper. Contribution 981201 of the Netherlands Research School of Sedimentary Geology (NSG).

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