An ebb-tide delta depositional model—a comparison between the modern Eastern Scheldt tidal basin (southwest Netherlands) and the Lower Eocene Roda Sandstone in the southern Pyrenees (Spain)

Yang, Chang‐Shu; Nio, S.D.

doi:10.1016/0037-0738(89)90091-2

Cited by 55 publications

(34 citation statements)

References 7 publications

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“…In wave-or tide-dominated settings, sediments are reworked and redistributed by basinal processes away from the river mouth, both alongshore and across-shelf (e.g., Yang and Nio, 1989). Wave-dominated coastal environments, in particular, consists of alternations of erosional stretches and accretive shore-parallel clinothems in plan-view (e.g., wave-dominated deltas, shorelines/beaches, strandplains, spits, barrier islands and cheniers) (Augustinus, 1978;Morales, 1997;Heward, 1981;Jiménez et al, 1997;Jol et al, 1996Jol et al, , 2002Bhattacharya and Giosan, 2003;Rasmussen, 2009).…”

Section: Delta Scale 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

198

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: Delta Scale 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

198

166

View full text Add to dashboard Cite

show abstract

“…Variation of dip angle from low-angle (13-14°) to high-angle (23-30°) in a distance of less than 30 m can be observed within the northern outcrops of Roda Y1 (Fig. 9C) (Yang and Nio, 1989;Nio and Yang, 1990). Cross-sets are up to 20 m thick and can be traced for up to 150 m (Figs.…”

Section: Fa 1b: Large-scale Cross-bedded Sandstonesmentioning

confidence: 88%

“…This latter interpretation was also used by several studies to follow (Puigdefabregas and Souquet, 1986;Crumeyrolle et al, 1992;Lopez-Blanco, 1996;Lopez-Blanco et al, 2003;Tinterri, 2007). In contrast, Yang and Nio (1989), and Yang (1990, 1991b), documented tidal bundles found in the southernmost outcrops of the Roda X and Roda Y units and interpreted the Roda U-Y units, as giant transverse tidal sand-bars at the mouth a NNE-SSW oriented estuary fed by a braided river. Five subunits differentiated within Roda Y were attributed to ebb-tidal delta lobes deposited at the estuary mouth or in meandering tidal channels as tidal point bars.…”

Section: Previous Workmentioning

confidence: 91%

“…grained sandstones and conglomeratic sandstones embedded in thick marlstone intervals, interpreted as distributary channel and mouthbar deposits of a sub-to supratidal, tide and storm-dominated fandelta and alluvial fan system (Yang and Nio, 1989;Molenaar and Martinius, 1996). The uppermost formations in the Ager Group are the San Esteban and Castigaleu formations ( Fig.…”

Section: Eocene Stratigraphy Along Isabena Valleymentioning

confidence: 98%

“…The thrust gave rise to a broad syncline acting as the depocentre for the "piggyback" basin. The westward deepening basin was a flat and shallow, bay-like marine-terrestial trough, 20 km wide and 95 km long in the axial ESE-WNW direction (Nijman and Nio, 1975;Yang and Nio, 1989).…”

Section: Regional Settingmentioning

confidence: 99%

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