Depositional sequences controlled by high rates of sediment supply, sea-level variations, and growth faulting: the Quaternary Baram Delta of northwestern Borneo

Hiscott, R.N.

doi:10.1016/s0025-3227(01)00118-9

Cited by 81 publications

(54 citation statements)

References 19 publications

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“…Similarly, in offshore studies, the seismic and acoustic profiles reveal the unconformities quite clearly (Hiscott, 2001;Virtasalo et al, 2005). In mountainous regions, the differences in elevation of the glacial deposits have facilitated delimitation of the allostratigraphic units in the field (cf.…”

Section: Allostratigraphy In Quaternary Depositsmentioning

confidence: 82%

A shift from lithostratigraphic to allostratigraphic classification of Quaternary glacial deposits

Räsänen

Auri²,

Huitti³

et al. 2009

Gsa Today

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The bedrock of the northern halves of North America and Europe is covered by Quaternary glacial deposits, forming a surficial overburden that is relatively thin, nonlithified, lithologically variable on a small scale (in terms of grain-size, mineralogy, texture, fabric, structure, and color), and often has a well-preserved depositional topography. These geologically unique characteristics and the fact that the glacial overburden was long considered to be of only restricted economic value have caused it to be treated differently in geological research from the older, regularly lithified strata. Due to the striking geomorphology of these glacial deposits, their investigation has also been incorporated into physical geography research. Thus, the segregation of the Quaternary research community into different schools of geology and geography has created multiple classification approaches and has caused the formal stratigraphic classifications successfully applied in pre-Quaternary geology to be applied less regularly to Quaternary glacial strata. This has led to inefficient use of Quaternary geological data for scientific and socio-economic purposes.The few currently existing national Quaternary stratigraphic frameworks are based on lithostratigraphy. These are poorly suited for describing deposits in glaciated shield areas in particular; we propose a classification for such areas based on the combined use of allostratigraphic and lithostratigraphic data, with alloformations as the fundamental units and lithostratigraphic units filling out the framework where appropriate. This classification would provide a hierarchical framework for glaciogenic deposits that could potentially support stratigraphic information systems, databases, and digital spatial models more effectively than the traditional lithostratigraphic frameworks.

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Section: Allostratigraphy In Quaternary Depositsmentioning

confidence: 82%

A shift from lithostratigraphic to allostratigraphic classification of Quaternary glacial deposits

Räsänen

Auri²,

Huitti³

et al. 2009

Gsa Today

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“…19a), and are the only instances when «deltaic clinothems» can be as thick as 100s-1000s m (Suter and Berryhill Jr, 1985;Mayall et al, 1992;Sydow and Roberts, 1994;Morton and Suter, 1996;Steel et al, 2000Steel et al, , 2003Steel et al, , 2008Steel and Olsen, 2002;Sydow et al, 2003;Johannessen and Steel, 2005;Covault et al, 2009;Hubbard et al, 2010;Pellegrini et al, 2018). In particular, example of Quaternary continental-margin deltas include the Niger, Congo, Mississippi and Amazon deltas (Fisk et al, 1954;Short and Stauble, 1967;Damuth, 1994;Hiscott, 2001;Rodger et al, 2006;Peltier and Fairbanks, 2006).…”

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

confidence: 99%

“…Only major structural elements (e.g., ocean/continent boundaries) can form slopes as high as thousands of metres. As a consequence, our definition of "continental-margin (scale) clinoform" comprises even clinoforms with heights as little as 500 m, as long as they are initially produced by the long-term sedimentary mantling of slopes associated with the transition from continental to oceanic crust, possibly followed by active "continental margin-delta" accretionary phases (see later) (Austin and Uchupi, 1982;Rice and Shade, 1982;Dillon et al, 1983;Larter and Barker, 1989;Hiscott, 2001;Walsh and Nittrouer, 2003;Lin et al, 2008;Houseknecht et al, 2009;Covault et al, 2009;Hubbard et al, 2010). This primary conditioning of continental-margin (scale) clinoform relief from geodynamics rather than sedimentary processes separates this clinoform class from the previous ones (including shelf-edge clinoforms), which are rarely associated directly with continental margins, active tectonics or structural lineaments (Steel and Olsen, 2002).…”

Section: Continental Margin Scale Clinoformsmentioning

confidence: 99%

“…Finally, if the shelf-edge delta reaches the continental margin (i.e. the edge of a whole continental shelf), a hybrid "continental margin delta" is created (e.g., present-day Niger, Congo, Mississippi and Amazon deltas -Fisk et al, 1954;Short and Stauble, 1967;Damuth, 1994;Hiscott, 2001;Rodger et al, 2006;Peltier and Fairbanks, 2006) (see Section 2.3.2).…”

Section: Spatial Associations Of Coeval Clinoforms: Compound Versus Hmentioning

confidence: 99%

“…(Legler et al, 2013) Jones et al, 2013;Pellegrini et al, 2018). This includes large-scale sediment transfer to the basin-floor of continental-margin clinoforms (e.g., oceanic abyssal plains), as in the Niger Delta and the Cretaceous Tres Pasos-Dorotea formations, Chile (Uchupi, 1968;Damuth, 1994;Hiscott, 2001;Covault et al, 2009;Hubbard et al, 2010). More generally, in continental-margin clinoforms, only negligible river-derived sediment transport towards the abyssal plain takes place, particularly during highstands (e.g., < 5% in the Recent Gulf of Papua), but the presence of submarine canyons extending in proximity of river mouths changes dramatically this sediment balance (e.g., about 90% of Recent sediment off the Sepik River) (Walsh and Nittrouer, 2003;Sweet and Blum, 2016).…”

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

187

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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Sedimentology

Liu¹,

Huang²,

Li³

et al. 2009

The South China Sea

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Depositional sequences controlled by high rates of sediment supply, sea-level variations, and growth faulting: the Quaternary Baram Delta of northwestern Borneo

Cited by 81 publications

References 19 publications

A shift from lithostratigraphic to allostratigraphic classification of Quaternary glacial deposits

A shift from lithostratigraphic to allostratigraphic classification of Quaternary glacial deposits

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

Sedimentology

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