Distribution of soft-sediment deformation structures in clinoform successions of the Permian Ecca Group, Karoo Basin, South Africa

Oliveira, Carlos M. M.; Hodgson, David M.; Flint, Stephen S.

doi:10.1016/j.sedgeo.2010.09.011

Cited by 55 publications

(37 citation statements)

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“…3) contains an approximately 1.8 km thick succession of deep-marine deposits . Grecula et al, 2003;Figueiredo et al 2009;Hodgson et al, 2011a;Spychala et al, 2015) to wave-dominated shelf and shelf-edge deposits (the ~350 m-thick Waterford Formation, Oliveira et al, 2011, Jones et al, 2013Fig. 3).…”

Section: Regional Settingmentioning

confidence: 98%

Palinspastic restoration of an exhumed deepwater system: A workflow to improve paleogeographic reconstructions

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Section: Regional Settingmentioning

confidence: 98%

Palinspastic restoration of an exhumed deepwater system: A workflow to improve paleogeographic reconstructions

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“…As a consequence of this growth style, shelf-edge clinothems typically possess a bipartite lithology, reflecting alternate sourcing by starved hemipelagic-hyperpycnal mud-drapes and, during shelf-edge delta stages, by active mud-or sand-prone shoreline progradation Bhattacharya and MacEachern, 2009). Several published case studies detail this relationship between shelfedge clinoforms and superimposed delta-scale clinoform cycles (e.g., Oliveira et al, 2011). For example, the Eocene-age succession outcropping in Spitsbergen hosts both gently-dipping low-relief (tens of metres) shoreline clinoforms and more steeply-dipping (3-6°), highrelief (average 200 m) sandy shelf-edge clinoforms.…”

Section: Shelf-edge Scale Clinoforms (Figs 14-16)mentioning

confidence: 99%

Clinoforms and clinoform systems: Review and dynamic classification scheme for shorelines, subaqueous deltas, shelf edges and continental margins

Patruno

Helland‐Hansen

2018

Earth-Science Reviews

200

166

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A B S T R A C TClinoforms are inclined and normally basinward-dipping horizons developed over a range of spatial and temporal scales in both siliciclastic and carbonatic systems. The study of clinoform successions underpins sequence stratigraphy and all efforts to reconstruct the relative partitioning of reservoir, seal and source rocks along shoreline to basin-floor profiles.Here, we review clinoform research and propose a more systematic description and classification of clinoforms. This is a crucial step to improve predictions of facies and lithology distribution within shoreline to continental shelf and abyssal plain successions, together with the genesis, drivers and dynamics of their constituent sedimentary units.Four basic clinoform types are here distinguished in delta/shorelines, lacustrines and marine environments, on the basis of their overall spatial and temporal scale, morphology, outbuilding dynamic and geodynamic and depositional setting: (1, 2) delta-scale clinoforms, which in turns are sub-divided into shoreline and delta-scale subaqueous clinoforms; (3) shelf-edge clinoforms; and (4) continental-margin clinoforms. Delta-scale clinoform sets are tens of metres high and typically represent 1-10 3 kyr, with progradation rates ranging from 1,000-100,000 m/kyr for shorelines and "subaerial deltas" to 100-20,000 m/kyr for subaqueous deltas; shelfedge clinoform sets are hundreds of metres high and are nucleated and accreted in 0.1-20 Myr (usual progradation rates of 1-100 m/kyr) by successive cross-shelf transits of delta-scale clinoforms; continental-margin clinoform sets are thousands of metres high, hallmark key geodynamic/crustal boundaries (e.g., continent/ocean transition) and slowly prograde basinwards in ca. 5-100 Myr, with typical rates of 0.1-10 m/kyr. As a consequence of the very different progradation rates and of the difficulty of large-scale clinothems to backstep during transgressions, shorelines are the most dynamic clinoforms with regards to position, continental margins the least, and shelf-edges are intermediate. Shortly after a transgression, therefore, the four clinoform types may prograde synchronously along shoreline-to-abyssal plain transects, forming "compound clinoform" systems. During the subsequent regressive cycle, however, due to the dissimilarity in progradation rates, different clinoform types will normally merge progressively with each other, giving rise to "hybrid clinoforms" (e.g., shelf-edge deltas), and fewer depositional breaks-in-slope are distinguished along a single shoreline-toabyssal plain transect. Overall, all clinoform systems are the result of the dynamic evolution of compound and hybrid clinoforms along a temporal and spatial continuum, regulated by the cyclical backstepping of the smallerscale system within natural progradational-retrogradational cycles of larger-scale clinothem outbuilding.All clinothem types may show either an accretionary/active or draping/passive style, depending on the proximity to the sediment source. Draping clinothems are nearly...

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“…The contemporaneous effects of cyclic loading, storm waves, and overloading have been proposed as an explanation for the SSDS in the lacustrine sediments (Martel and Gibling 1993). SSDS resulting from liquefaction and fluidization in fluviolacustrine and deltaic environments have been reported by many authors (Sims 1973(Sims , 1975Gill and Kuenen 1957;Gill 1979;Hesse and Reading 1978;Coleman and Lindsay 1983;Suter and Berryhill 1985;Eyles and Clark 1986;Mayall et al 1992;Martel and Gibling 1993;Rodrıǵuez-Pascua et al 2000;Mellere et al 2002;Tanner and Lucas 2010;Oliveira et al 2011;Pisarska-Jamroży and Weckwerth 2013). Field analyses and modelling on the liquefaction and fluidization processes induced by rapid sedimentation in lacustrine, delta, and offshore marine environments are often associated with turbidity currents.…”

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“…Their experiments resulted in asymmetrical pillow structure and elongated sets of load casts. Haughton et al (2009), Oliveira (2008, unpublished Ph.D. thesis), Oliveira et al (2011), Sumner et al (2012) considered SSDS to be common components of turbiditic successions.…”

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“…For example, Lee et al (2014) studied bedding features and relations of coastal settings bearing SSDS and interpreted the origin of SSDS to be a consequence of seismic events related to active faults. Aseismic deformations were interpreted by many authors: Oliveira et al (2009), Tanner and Lucas (2010), Oliveira et al (2011) or Chen and Lee (2013), and seismic deformations by Ricci Lucchi (1995), Rossetti (1999), Rodrıǵuez-Pascua et al (2000), Rossetti and Góes (2000), Moretti et al (2002), Brandes andWinsemann (2013).…”

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Types of soft-sediment deformation structures in a lacustrine Ploužnice member (Stephanian, Gzhelian, Pennsylvanian, Bohemian Massif), their timing, and possible trigger mechanism

Stárková

Martínek

Mikuláš

et al. 2015

Int J Earth Sci (Geol Rundsch)

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facies associations preserve from 22.5 to 20.5 cm SSDS/m, and in palustrine carbonate, 13.5 cm mechanical SSDS/m was found. SSDS in fluvial facies are rare (2.9 cm SSDS/m). The distribution of SSDS in the Sm-1 borehole shows clear relationships to sedimentary facies and processes such as density flows or fluctuation of water level. The relationships of particular structures indicate a relative timing of formation which is as follows: sediment deposition was followed by the formation of mechanical SSDS, then by bioturbation, and finally by deformations due to early diagenetic growth of carbonates and silica. The distribution of SSDS in vertical sections and their direct relationship to sedimentary facies point to endogenic rather than external trigger mechanisms such as seismic activity. The main endogenic trigger mechanisms responsible for the origin of SSDS included a Stephanian semi-humid seasonal climate, basin morphology with relatively steep gradients, and elevated source areas, which created a conducive environment for rapid and repeated deposition of sheetfloods and hyperconcentrated flows and turbidites causing syndepositional loading.

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Distribution of soft-sediment deformation structures in clinoform successions of the Permian Ecca Group, Karoo Basin, South Africa

Cited by 55 publications

References 48 publications

Palinspastic restoration of an exhumed deepwater system: A workflow to improve paleogeographic reconstructions

Palinspastic restoration of an exhumed deepwater system: A workflow to improve paleogeographic reconstructions

Clinoforms and clinoform systems: Review and dynamic classification scheme for shorelines, subaqueous deltas, shelf edges and continental margins

Types of soft-sediment deformation structures in a lacustrine Ploužnice member (Stephanian, Gzhelian, Pennsylvanian, Bohemian Massif), their timing, and possible trigger mechanism

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