A highstand shelf-margin delta system from the Eocene of West Spitsbergen, Norway

Uroza, Carlos Alberto; Steel, Ronald J.

doi:10.1016/j.sedgeo.2007.12.003

Cited by 84 publications

(71 citation statements)

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“…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. Regressive-transgressive shoreline cycles across narrow (1-10 km) and shallow (< 50 m) shelves are reflected by the alternate deposition of actively accreting sand-prone shelf-edge delta clinothems and, after each transgression, mudstone-prone shelf-edge draping clinothems (HellandHansen, 1992(HellandHansen, , 2010Helland-Hansen et al, 1994;Steel et al, 2000Steel et al, , 2003Steel and Olsen, 2002;Mellere et al, 2002;Johannessen and Steel, 2005;Uroza and Steel, 2008;Johannessen et al, 2011;Grundvåg et al, 2014) (Fig. 14D).…”

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

confidence: 99%

“…During normal regression (i.e., ascending clinoform trajectories), in contrast, continental-margin and shelf-edge deltas are normally associated with aggradational wave-dominated clinoforms that are near-linear in planview, lack focused sediment dispersal and, in the absence of gullied shelf-edges, are characterised by slopes that are either mudstone-prone or host only minor tempestite sheet sandstones, and by negligible or muddy submarine fan development (Kolla et al, 2000;Steel and Olsen, 2002;Steel, 2002, 2006;Deibert et al, 2003;Ritchie et al, 2004aRitchie et al, , 2004bBullimore et al, 2005;Johannessen and Steel, 2005;Porębski and Steel, 2006;Uroza and Steel, 2008;Gong et al, 2015;Gong et al, 2015;c.f. also the c2 clinothem of the upper Pleistocene Po-Adriatic succession, as detailed in Pellegrini et al, 2018).…”

Section: Shelf-edge Delta and Continental-margin Delta Hybrid Clinoformsmentioning

confidence: 99%

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

confidence: 99%

Section: Shelf-edge Delta and Continental-margin Delta Hybrid Clinoformsmentioning

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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“…These consisted in all cases either of chert or quartz/quartzite. The boundary between the Basilika Formation and the overlying Grumantbyen Formation is well exposed and FIGURE 4 | Paleogene stratigraphy of the Central Tertiary Basin of Spitsbergen (modified from Steel et al, 1985;Uroza and Steel, 2008;Charles et al, 2011). marked by the occurrence of a fine-grained glauconitic sandstone bed.…”

Section: Sampling and Field Observationsmentioning

confidence: 99%

Origin of Bentonites and Detrital Zircons of the Paleocene Basilika Formation, Svalbard

et al. 2016

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The Paleocene was a time of transition for the Arctic, with magmatic activity of the High Arctic Large Igneous Province (HALIP) giving way to magmatism of the North Atlantic Large Igneous Province in connection to plate tectonic changes in the Arctic and North Atlantic. In this study we investigate the Paleocene magmatic record and sediment pathways of the Basilika Formation exposed in the Central Tertiary Basin of Svalbard. By means of geochemistry, Sm-Nd isotopic signatures, and zircon U-Pb geochronology we investigate the characteristics of several bentonite layers contained in the Basilika Formation, as well as the provenance of the intercalated clastic sediments. Our data show that the volcanic ash layers of the Basilika Formation, which were diagenetically altered to bentonites, originate from alkaline continental-rift magmatism such as the last, explosive stages of the HALIP in North Greenland and the Canadian Arctic. The volcanic ash layers were deposited on Svalbard in a flat shelf environment with dominant sediment supply from the east. Dating of detrital zircons suggests that the detritus was derived from Siberian sources, primarily from the Verkhoyansk Fold-and-Thrust Belt, which would require transport over ∼3000 km across the Arctic.

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“…Uroza & Steel 2008), demonstrates that rigorous application of 'standard' sequence stratigraphic models (which for didactic purposes have B. LEVELL ET AL.…”

Section: Shelf Edge Deltas and Playsmentioning

confidence: 99%

Passive margins: overview

Levell

Argent

Doré³

et al. 2010

PGC

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Passive margins have been the reliable, accessible mainstay of exploration success worldwide for the last 25 years, and have hosted the spectacularly fast exploitation of deepwater resources (Angola, Nigeria, Brazil, Trinidad, USA Gulf of Mexico, Egypt, Australia and India). Despite, or perhaps because of this, there is still much to learn about the variety of hydrocarbon habitats they present.For example: (1) deep seismic observations and deep sea drilling have revealed more of the diversity of passive margins geodynamics. This liberates explorationists from simple geodynamic models, with consequences not only for new views of thermal history but also for the whole tectonic and stratigraphic evolution. For example, the time significance assigned to the geometries traditionally labelled 'pre-rift, syn-rift and sag' may be misleading. This has implications for correlations, the significance assigned to unconformities and sequence boundaries, heat flow and structural history. (2) New deep imaging of the sedimentary sections has revealed mistaken assumptions about the importance of 'mobile substrate' in major deltas and allowed the detailed unravelling of salt and shale movement and its implications for reservoir and trap. (3) Depositional models for deepwater reservoirs have increased in predictive capability and modern seismic imaging supports new models for shallow water sequences. (4) Discoveries of very large amounts of dry bacterial methane in stratigraphic traps have challenged old assumptions about prospectivity based on thermally matured source rocks. (5) New engineering and development technologies are opening up the commercialization of remote frontiers. As a consequence there is legitimate scope to re-visit old 'dogmas' and to propose that each passive margin segment is best regarded as unique, with analysis and interpretation rooted in observation rather than models (at least while the newly proposed models evolve to stability). Many of these themes were visited in the Passive Margins session of the Seventh Petroleum Geology Conference, held in London in 2009. This paper outlines some of these ideas, and considers how exploration along passive margins in the next decade can use new geoscience thinking.

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A highstand shelf-margin delta system from the Eocene of West Spitsbergen, Norway

Cited by 84 publications

References 50 publications

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

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

Origin of Bentonites and Detrital Zircons of the Paleocene Basilika Formation, Svalbard

Passive margins: overview

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