The Sticklepath-Lustleigh fault zone: Tertiary sinistral reactivation of a Variscan dextral strike-slip fault

Holloway, S.; Chadwick, R. A.

doi:10.1144/gsjgs.143.3.0447

Cited by 64 publications

(32 citation statements)

References 28 publications

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“…Further reactivation of NNW-SSE faults occurred during the Oligocene-Miocene intraplate shortening (Holloway and Chadwick 1986) that was…”

Section: Episodic Intraplate Rifting and Inversion (Late Permian -Cenmentioning

confidence: 99%

Indium mineralisation in SW England: Host parageneses and mineralogical relations

Stickland

Rollinson

Shail

2016

Ore Geology Reviews

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“…Further reactivation of NNW-SSE faults occurred during the Oligocene-Miocene intraplate shortening (Holloway and Chadwick 1986) that was…”

Section: Episodic Intraplate Rifting and Inversion (Late Permian -Cenmentioning

confidence: 99%

Indium mineralisation in SW England: Host parageneses and mineralogical relations

Stickland

Rollinson

Shail

2016

Ore Geology Reviews

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“…2; the high density of this material can increase the strength of gravity by tens of parts per million). Also in the Eocene, the Sticklepath-Lustleigh fault zone, which crosses southwest England between the Bideford and Torquay areas, became reactivated in a left-lateral sense (this NW-SE-trending fault zone originally developed with rightlateral slip during the Variscan orogeny; Holloway and Chadwick, 1986). Two onshore sedimentary basins, the Bovey Basin (NW of Newton Abbot) and the Petrockstow Basin farther northwest, developed at leftward steps in this fault zone and formed significant subaerial depocentres, lasting into the Oligocene, for fluvial and lacustrine sands and clays (the Stanley Bank Basin, indicating a similar palaeoenvironment, is now offshore, east of Lundy; the Bovey Basin succession is documented by Selwood et al, 1984).…”

Section: Introductionmentioning

confidence: 99%

Cenozoic uplift of southwest England

Westaway

2010

J Quaternary Science

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The uplift history of southwest England is inferred using a composite dataset including marine and fluvial terraces and karstic data. The estimated post-Mid-Pliocene uplift increases eastward from $130 m in west Cornwall and $135 m in south Devon to $150 m in the Hampshire Basin. The post-Early-Pleistocene uplift likewise increases eastward, from $55 m in west Cornwall to $60 m in south Devon and $80 m in Hampshire. Landscape and thermochronological evidence also indicates Eocene uplift, caused by the British Tertiary Igneous Province magmatism; this component tapers eastward from $300 m in west Cornwall to $50 m in south Devon, with subsidence in east Devon. This uplift accompanied magmatic underplating; the mafic layer added to the basal crust thins eastward from $6 km in west Cornwall to $2 km in south Devon, evidently tapering to zero farther east. The laterally variable crustal properties caused by this variation in underplating have affected the post-MidPliocene uplift; the study region is thus intermediate, in terms of crustal strength and landscape evolution, between central-southern England, with no underplating, and Ireland, where $10 km thick underplating has resulted in extreme Late Cenozoic landscape stability. The Eocene mantle-plumerelated uplift is distinct from the post-Mid-Pliocene phase which, the modelling indicates, has been driven by surface processes and, thus, by climate change.

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“…Normal faults dip either north or south to divide the basin into fault blocks (Dart et al, 1995). The basin was inverted in the Eocene and Oligocene during a period of N±S compression associated with Alpine tectonics (Holloway and Chadwick, 1986;Arthur, 1989;Dart et al, 1995;Nemcok et al, 1995). Alpine deformation was accommodated by reverse-reactivation of normal faults, new thrust faults, new strike-slip faults, and by hanging wall buttress anticlines.…”

Section: Introductionmentioning

confidence: 99%

Joint development normal to regional compression during flexural-flow folding: the Lilstock buttress anticline, Somerset, England

Engelder

Peacock

2001

Journal of Structural Geology

102

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Alpine inversion in the Bristol Channel Basin includes reverse-reactivated normal faults with hanging wall buttress anticlines. At Lilstock Beach, joint sets in Lower Jurassic limestone beds cluster about the trend of the hinge of the Lilstock buttress anticline. In horizontal and gently north-dipping beds, J 3 joints ( 295±2858 strike) are rare, while other joint sets indicate an anticlockwise sequence of development. In the steeper south-dipping beds, J 3 joints are the most frequent in the vicinity of the reverse-reactivated normal fault responsible for the anticline. The J 3 joints strike parallel to the fold hinge, and their poles tilt to the south when bedding is restored to horizontal. This southward tilt aims at the direction of s 1 for Alpine inversion.Finite-element analysis is used to explain the southward tilt of J 3 joints that propagate under a local s 3 in the direction of s 1 for Alpine inversion. Tilted principal stresses are characteristic of limestone±shale sequences that are sheared during parallel (¯exural-¯ow) folding. Shear tractions on the dipping beds generate a tensile stress in the stiffer limestone beds even when remote principal stresses are compressive. This situation favors the paradoxical opening of joints in the direction of the regional maximum horizontal stress. We conclude that J 3 joints propagated during the Alpine compression caused the growth of the Lilstock buttress anticline. q 2001 Published by Elsevier Science Ltd. IntroductionAn old paradigm is that outer-arc stretching leads to foldrelated jointing (Van Hise, 1896). Outer-arc stretching is associated with tangential longitudinal strain folds that develop when a homogeneous, isotropic layer is buckled (Price and Cosgrove, 1990). The tangential longitudinal strain fold is divided by a neutral surface beyond which the inner arc of the fold is compressed. Joints that initiate in the outer arc of anticlines propagate down to but do not cross the neutral surface. When fold-related jointing penetrates the entire thickness of a bed, the tangential longitudinal strain model is less useful as a mechanism to explain the strain that may have caused jointing. This is also true when jointing is well developed in the limbs of folds or at in¯ection points where strain goes to zero in a tangential longitudinal strain fold. To understand the development of jointing in the limbs of folds, we must look to another model. Flexural¯ow folds have maximum strains at the in¯ection points and zero strain at the hinges (Price and Cosgrove, 1990).We consider the possibility that one or more sets of un®lled joints of the Bristol Channel were contemporaneous with¯exural-¯ow folding during Alpine shortening. Here, we describe ®eld data gathered to test this hypothesis. We presume that the joint geometries interpreted to date from the Alpine inversion re¯ect the superposition of local and remote (i.e. regional) stress conditions. We also use the orientation of systematic joints in carbonate beds to constrain a mechanical model for stress dis...

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The Sticklepath-Lustleigh fault zone: Tertiary sinistral reactivation of a Variscan dextral strike-slip fault

Cited by 64 publications

References 28 publications

Indium mineralisation in SW England: Host parageneses and mineralogical relations

Indium mineralisation in SW England: Host parageneses and mineralogical relations

Cenozoic uplift of southwest England

Joint development normal to regional compression during flexural-flow folding: the Lilstock buttress anticline, Somerset, England

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