Hanging wall fault kinematics and footwall collapse in listric growth fault systems

Imber, Jonathan B.; Childs, Conrad; Nell, P.A.R.; Walsh, John J.; Hodgetts, David; Flint, Stephen S.

doi:10.1016/s0191-8141(02)00034-2

Cited by 52 publications

(55 citation statements)

References 25 publications

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“…10j). This variability contrasts previous studies that have documented either a general seaward-propagating trend of consecutive deltaic growth structures (e.g., Evamy et al, 1978;Rider, 1978;Bruce, 1983;McClay et al, 2003), or a retrogradation of bounding faults into previously undeformed footwall terrain (e.g., Gibbs, 1984;Vendeville, 1991;Bhattacharya and Davies, 2001;Imber et al, 2003;Back et al, 2006).…”

Section: Discussioncontrasting

confidence: 92%

“…The backstepping of deltaic faults into former footwall terrain, as observed in the southeast of the study area, has been related previously to gravity-induced failure along prominent fault scarps bounding underfilled basins (e.g., Gibbs, 1984;Hesthammer and Fossen, 1999), to footwall collapse above rising diapirs (e.g., Morley and Guerin, 1996;Imber et al, 2003), or to fault segment linkage by footwall breaching (e.g., Peacock and Sanderson, 1991;Trudgill and Cartwright, 1994;Childs et al, 1995;Imber et al, 2003;Fazli Khani and Back, 2012). In the study area, gravityinduced failure can be excluded as an explanation for fault backstepping as there is no evidence for a fault-scarp paleotopography or for sedimentary underfill.…”

Section: Discussionmentioning

confidence: 70%

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The influence of pre-existing structure on the growth of syn-sedimentary normal faults in a deltaic setting, Niger Delta

Khani

Back

2015

Journal of Structural Geology

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Section: Discussioncontrasting

confidence: 92%

Section: Discussionmentioning

confidence: 70%

The influence of pre-existing structure on the growth of syn-sedimentary normal faults in a deltaic setting, Niger Delta

Khani

Back

2015

Journal of Structural Geology

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“…Koyi and Skelton 2001;Imber et al 2003;Krézsek et al 2007). Our simple restoration of the extensional fault in St. Margarethen does not result in a geologically plausible sub-horizontal lower part of a listric fault.…”

Section: Listric Versus Planar Fault Geometrymentioning

confidence: 99%

Listric versus planar normal fault geometry: an example from the Eisenstadt-Sopron Basin (E Austria)

Spahić

Exner

Behm

et al. 2010

Int J Earth Sci (Geol Rundsch)

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In a gravel pit at the eastern margin of the Eisenstadt-Sopron Basin, a satellite of Vienna Basin (Austria), Neogene sediments are exposed in the hanging wall of a major normal fault. The anticlinal structure and associated conjugated secondary normal faults were previously interpreted as a rollover anticline above a listric normal fault. The spatial orientation and distribution of sedimentary horizons and crosscutting faults were mapped in detail on a laser scan of the outcrop wall. Subsequently, in order to assess the 3D distribution and geometry of this fault system, a series of parallel ground penetrating radar (GPR) profiles were recorded behind the outcrop wall. Both outcrop and GPR data were compiled in a 3D structural model, providing the basis for a kinematic reconstruction of the fault plane using balanced cross-section techniques. However, the kinematic reconstruction results in a geologically meaningless normal fault cutting downand up-section. Additionally, no evidence for a weak layer serving as ductile detachment horizon (i.e. salt or clay horizon) can be identified in stratigraphic profiles. Instead, the observed deflection of stratigraphic horizons may be caused by a displacement gradient along a planar master fault, with a maximum displacement in the fault centre, decreasing towards the fault tips. Accordingly, the observed deflection of markers in the hanging wall-and in a nearby location in the footwall of the normal fault-is interpreted as large-scale fault drag along a planar fault that records a displacement gradient, instead of a rollover anticline related to a listric fault.

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“…The resulting succession of deltaic, inters lope and abyssal plain deposits has reached a thickness of approximately 12 km [1]. Deltaic growth faults and associated strata record the interaction between sedimentary processes and fault movements, and as such they are good for detailed studies of the interaction of tectonics and sedimentation [8][9][10][11][12]. Structure and depositional systems have migrated with the progradation of the delta through time.…”

Section: Introductionmentioning

confidence: 99%

Structural Deformation and Depositional Processes: Insights from the Greater Ughelli Depobelt, Niger Delta, Nigeria

Obiadi¹,

Cm²

2016

Oil Gas Res

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The growth and development of the structural and depositional systems in the hydrocarbon rich Niger Delta, off the Atlantic Coast of Nigeria, West Africa, involves a complex interaction of extension, contraction and subsidence such that at any given point in time up-dip extensional system are kinematically linked to down-dip contractional systems via a transitional zone. On the regional tectonostratigraphic zonation are local structural and depositional systems associated with individual extensional faults and thrust-cored folds, local subsidence and withdrawal associated with shale diapir growth. The research is a case study of growth faults and associated deltaic sedimentation in the Greater Ughelli Depobelt of the Niger Delta. Using 3D seismic, a range of well log suites and biostratigraphic data, a regional sequence stratigraphic framework of the study area was produced. Six Maximum Flooding Surfaces MFS's and five Sequence Boundaries SB's were defined within the confines of available data. With the aid of these regional horizons/markers (MFSs and SBs) and events pattern in the seismic volume, a structural interpretation model and framework for the study area was also undertaken. Structural analysis show that fault activity began well before 31.3 Ma and continued beyond 20.7 Ma, and has greatly influenced the creation of accommodation space and sediment accumulation. Generally, due to structural deformation and structurally induced accommodation creation, stratigraphic thickness is observed to have increased in the basin ward direction, and at different stages in the structural evolution of the study area, 'local depocenter' have migrated to the NW (29.3 Ma-22.2 Ma) and then to the SE (22.2 Ma-20.7 Ma) resulting also in lateral changes in stratigraphic thicknesses in these directions.

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Hanging wall fault kinematics and footwall collapse in listric growth fault systems

Cited by 52 publications

References 25 publications

The influence of pre-existing structure on the growth of syn-sedimentary normal faults in a deltaic setting, Niger Delta

The influence of pre-existing structure on the growth of syn-sedimentary normal faults in a deltaic setting, Niger Delta

Listric versus planar normal fault geometry: an example from the Eisenstadt-Sopron Basin (E Austria)

Structural Deformation and Depositional Processes: Insights from the Greater Ughelli Depobelt, Niger Delta, Nigeria

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