Late syn‐rift evolution of the Vingleia Fault Complex, Halten Terrace, offshore Mid‐Norway; a test of rift basin tectono‐stratigraphic models

Abstract

Rift basin tectono-stratigraphic models indicate that normal fault growth controls the sedimentology and stratigraphic architecture of syn-rift deposits. However, such models have rarely been tested by observations from natural examples and thus remain largely conceptual. In this study we integrate 3D seismic reflection, and biostratigraphically constrained core and wireline log data from the Vingleia Fault Complex, Halten Terrace, offshore Mid-Norway to test rift basin tectono-stratigraphic models. The geometry of the basin-bounding fault and its hangingwall, and the syn-rift stratal architecture, vary along strike. The fault is planar along a much of its length, bounding a half-graben containing a faultward-thickening syn-rift wedge. Locally, however, the fault has a ramp-flat-ramp geometry, with the hangingwall defined by a fault-parallel anticline-syncline pair. Here, an unusual bipartite syn-rift architecture is observed, comprising a lower faultward-expanding and an upper faultward-thinning wedge. Fine-grained basinfloor deposits dominate the syn-rift succession, although isolated coarse clastics occur. The spatial and temporal distribution of these coarse clastics is complex due to syn-depositional movement on the Vingleia Fault Complex. High rates of accommodation generation in the fault hangingwall led to aggradational stacking of fan deltas that rapidly (<5 km) pinch out basinward into offshore mudstone. In the south of the basin, rapid strain localization meant that relay ramps were short-lived and did not represent major, long-lived sediment entry points. In contrast, in the north, strain localization occurred later in the rift event, thus progradational shorefaces developed and persisted for a relatively long time in relay ramps developed between unlinked fault segments. The footwall of the Vingleia Fault Complex was characterized by relatively low rates of accommodation generation, with relatively thin, progradational hangingwall shorelines developed downdip of the fault block apex, sometime after the onset of sediment supply to the hangingwall. We show that rift basin tectono-stratigraphic models need modifying to take into account along-strike variability in fault structure and basin physiography, and the timing and style of syn-rift sediment dispersal and facies, in both hangingwall and footwall locations.

Unravelling key controls on the rift climax to post‐rift fill of marine rift basins: insights from 3D seismic analysis of the Lower Cretaceous of the Hammerfest Basin, SW Barents Sea

“…Variability along the strike of the main bounding faults : In this study, we consider the variability in the throw and the steps in the main bounding faults to be a factor affecting the depositional systems and the input of sediments into the basin, as it has been considered previously (Gawthorpe et al ., ; Gupta et al ., ; McLeod et al ., ; Elliott et al ., , ). High accommodation space was generated in faults with higher throw, for example in the southern bounding fault (TFFC).…”

“…The infill of marine rift basins is controlled by several variables: climate, eustatic sea-level, subsidence, drainage evolution, footwall lithology, nature of the feeder system (e.g. point source, multiple source or linear source), variability along the strike of the faults and basin physiography (Stow et al, 1996;Ravn as & Steel, 1998;Allen & Densmore, 2000;Gawthorpe & Leeder, 2000;McArthur et al, 2013;Sømme et al, 2013;Elliott et al, 2017). Some of these variables are determined by the evolution of fault propagation, which typically depends on the stage of the rift evolution (Cowie et al, 2000;Gawthorpe & Leeder, 2000).…”

“…Subsidence commonly outpaces sedimentation, resulting in the deposition of deep-marine mudstones with localized coarse clastic wedges deposited close to the footwall area (Leppard & Gawthorpe, 2006). Coarse-grained sediments have been described at the base of the fault scarp in slope aprons, slumps and slides, talus and coarse-grained aggradational or progradational fan deltas (Surlyk, 1978(Surlyk, , 1989Stow et al, 1996;Gawthorpe et al, 1997;Leppard & Gawthorpe, 2006;Larsen et al, 2010;Henstra et al, 2016;Elliott et al, 2017). Progradation tends to occur with low accommodation or high sediment supply or a combination of these factors (Gawthorpe & Leeder, 2000).…”

Characterizations and accumulation of lacustrine source rocks in the Zhu I Depression, Pearl River Mouth Basin, China

“…On the basis of the interpreted sequence stratigraphic framework of the Zhu I Depression, we selected SE–NW trending seismic profiles in the four sags to reveal the tectonic history and the controls on the deposition of the Wenchang Formation. Syn‐depositional faults can be interpreted in the seismic profiles based on the different thicknesses of the down‐thrown block and up‐thrown block (Elliott et al, ; Shi et al, ; Shi, Zhao, Jiang, Miao, & Wang, ; Warke & Schröder, ). Additionally, the array of faults can be interpreted based on their termination locations.…”

Evolution of drainage, sediment‐flux and fluvio‐deltaic sedimentary systems response in hanging wall depocentres in evolving non‐marine rift basins: Paleogene of Raoyang Sag, Bohai Bay Basin, China

“…These include drainages associated with the rift axis, drainages associated with the footwall and drainages associated with upthrown portions of the hanging wall dipslope (e.g., Gawthorpe & Leeder, 2000;Hsiao, Graham, & Tilander, 2010;Leeder, 2011;Masini, Manatschal, Mohn, Ghienne, & Lafont, 2011). Examples of such interactions include subsidence rate control on the location of axial depositional systems, or increased interactions of transverse depositional systems with axial depositional systems during the late syn-rift and post-rift stages (e.g., Bridge & Mackey, 1993;Elliott et al, 2015;Gawthorpe & Leeder, 2000;Leeder & Jackson, 1993;Leeder & Mack, 2001;Muravchik, Bilmes, & D'elia, 2014;Muravchik, Gawthorpe, & Sharp, 2018). Studies of these interactions have led to significant advances in understanding how clastic depositional systems distribute and evolve during different rift stages.…”