342:, slope topography, erosive base at flow onset and the effects of both lateral stacking and lateral accretion. Compared to their terrestrial cousins, the scale of submarine systems observed in seismic sections, aerial photos and rock outcrops are in no way comparable. As expected with this significant difference in scale, the dynamics of turbid current flows within submarine channels are significantly different from fluvial systems. These differences in dynamics and scale are due to the much lower density contrast between the flow and the host fluid is much lower in submarine channels than that of open channel flows with a free surface. This causes the flow to be significantly super-elevated about the channel margin causing overspill and building the levees.
282:, and the overbank passage of large flows not confined by the internal levees. As a consequence of lateral migration, internal levees may be better preserved on inner bends. Internal levees form only when confinement has been established, through the construction of external levees and/or the degradation and entrenchment of the composite erosion surface of the channel-belt, or confined within
27:
767:
350:
submarine channels can exhibit both lateral and vertical migration. Fluvial systems do not exhibit this vertical component. Lateral accretion packages are believed to form as a result of depositional rather than topographical forcing. This lateral migration only style of sinuosity is believed to be somewhat rare in occurrence within turbidite systems.
286:. Internal levees may form distinct wedges of sediment where enough space is available; where space is limited, i.e., where overspill from underfit channels interacts with external levees or erosional confinement, overspill deposits may appear superficially similar to terrace deposits, which are widely identified in the subsurface.
358:
causing a displaced incision. Mayall suggests that this vertical movement could be as a result of changes in seafloor topography due to salt/shale tectonics or fault movement. The other alternative they suggest is through undefined “depositional processes”. One potential process may be as a result of
325:
The sinuosity of submarine channels is a characteristic instantly recognizable as being shared with fluvial systems. In recent years there are increasingly mixed opinions in academic literature as to how far they are analogous to each other with some feeling that such notions of similarity should not
265:
forms during the evolution of a genetically related channel-belt (or slope valley, channel fairway) by flows that partially spill out of their confinement. External levees can confine adjacent channel belts to form levee-confined systems. External levees may be much less sinuous than the levees of an
372:
of flows along the channel. When Froude numbers are low (<1.0) channel widths remain constant, however when Froude number oscillate around unity, channel widths fall rapidly with channel-floor slope. This provides a mechanism for generating channel widths capable of maintaining near-critical flow
273:
Internal levees are constructional features fed by flows that partially spilled out of channelised confinement, but were largely unable to escape the confinement of the channel-belt. The flows which build internal levees may interact with the main confining surface, i.e., the external levees, and/or
194:
What constitutes a channel is not straight forward. Different terms are used on a per study basis, all of which have similar but not quite interchangeable definitions. There have been efforts to produce an up-to-date, holistic view, but even since then there has been a significant number of papers
349:
plays an important part in fluvial systems. It is the feature of submarine channels that is most analogous with its terrestrial counterpart. It consists of erosion on the outerbank and deposition on the inner bank as a point bar. However, there are significant dissimilarities the biggest in that
302:
associated with both channel sediments and surrounding deep water sediments. Although it is not always clear how these sinuosities evolve, they typically do not result from a random wandering. In most cases, the wandering and changes in sinuosity is as a result of external forces. As a result of
380:
crosses is inevitably going to affect the geometry of the channel. This can result in subtle changes in channel path to major diversions in channel flow. Topographic influences can come in the form of the surface expression of faults or changes in topography as a result of salt/shale tectonics,
367:
Aggradational channels commonly form where the slope is “below grade.” This results in the deposition of broad, amalgamated and highly sand rich channels which are significantly affected by the slope morphology. The channel width versus slope relationship is control by the
1144:
Arnott, R. W. C. (1 June 2007). "Stratal architecture and origin of lateral accretion deposits (LADs) and conterminuous inner-bank levee deposits in a base-of-slope sinuous channel, lower Isaac
Formation (Neoproterozoic), East-Central British Columbia, Canada".
326:
hold. The best description is that the two are similar in some ways but more variable and complex in other. This applies to both the geometry of morphological features, the processes involved in forming them as well as the character of the deposits formed.
158:. Submarine channels and the turbidite systems which form them are responsible for the accumulation of most sandstone deposits found on continental slopes and have proven to be one of the most common types of hydrocarbon reservoirs found in these regions.
353:
Vertical migration is exhibited in submarine channels systems in the form of channel stacking. As flows in channels subside, channels are infilled with sediment. When the flow is re-initiated, there is then a slight shift laterally in the flow
958:
Damuth, John E.; Flood, Roger D.; Kowsmann, Renato O.; belderson, Robert H.; Gorini, Marcus A. (1988). "Anatomy and growth pattern of amazon deep-sea fan as revealed by long-range side-scan sonar (GLORIA) and high-resolution seismic studies".
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systems and potentially is one of the leading controls in the formation of levee confined complexes. In terms of sinuosity, Mayall shows that this vertical migration occurs on the outward sides of bends reinforcing any pre-existing curvature.
581:
768:"Sedimentological criteria to differentiate submarine channel levee subenvironments: Exhumed examples from the Rosario Fm. (Upper Cretaceous) of Baja California, Mexico, and the Fort Brown Fm. (Permian), Karoo Basin, S. Africa"
321:
of between 1.2 and 1.15. Difficulty with rigorous application of these values is that relatively straight channels may locally exceed them and some sinuous channels may display peak sinuosity values well in excess.
253:
to avoid confusion in the literature concerning the use of "inner" and "outer" levees. To help encourage this unification of phrases into a clearer architectural hierarchy, this study will use Kane's nomenclature.
266:
individual channel-levee system as they do not follow one particular channel but may be the product of overspill from one or more channels or channel-levee systems meandering within the wider channel-belt. The
329:
Mike Mayall provides the best summary that discusses the causes of sinuosity. Factors involve: flow dynamics such as flow density and flow velocity; and the depth of the current relative to topography; and
633:
Gee, M. J. R.; Gawthorpe, R. L.; Friedmann, S. J. (1 January 2006). "Triggering and evolution of a giant submarine landslide, offshore angola, revealed by 3d seismic stratigraphy and geomorphology".
918:"Anatomy and evolution of a slope channel-complex set (Neoproterozoic Isaac formation, Windermere supergroup, southern Canadian cordillera): Implications for reservoir characterization"
270:
is the highest point of the external levee, and runs parallel to the course of the channel-belt, separating the external levees into outer external levees and inner external levees.
177:. This makes them one of several geological processes responsible for the transport of coarse-grained sediment into deep water, as well as being a chief conduit for the transfer of
1109:
Abreu, Vitor; Sullivan, Morgan; Pirmez, Carlos; Mohrig, David (1 June 2003). "Lateral accretion packages (LAPs): an important reservoir element in deep water sinuous channels".
173:
that may run for thousands of kilometres across the ocean floor. Often, they coalesce and overlap to form channel levee complexes which are the building blocks of many major
986:
Babonneau, N.; Savoye, B.; Cremer, M.; Bez, M. (1 January 2004). "Multiple terraces within the deep incised Zaire Valley (ZaĂŻAngo
Project): Are they confined levees?".
686:
1032:
Peakall, Jeff; McCaffrey, Bill; Kneller, Ben (1 May 2000). "A process model for the evolution, morphology, and architecture of sinuous submarine channels".
860:
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heterogeneous infilling of the older channel forming an offset conduit for later flows. Whatever the process this stacking plays an important role in
731:
Mayall, Mike; Jones, Ed; Casey, Mick (1 September 2006). "Turbidite channel reservoirs—Key elements in facies prediction and effective development".
545:
Bull, Suzanne; Cartwright, Joe; Huuse, Mads (1 August 2009). "A review of kinematic indicators from mass-transport complexes using 3D seismic data".
510:
Kane, Ian A.; McCaffrey, William D.; Peakall, Jeff (1 January 2010). "On the origin of paleocurrent complexity within deep marine channel levees".
1240:
917:
1224:
470:
Flood, Roger D.; Damuth, John E. (1 June 1987). "Quantitative characteristics of sinuous distributary channels on the Amazon Deep-Sea Fan".
373:
by channel narrowing and enhanced sedimentation. This behavior is controlled by an unknown constant that could not be found experimentally.
416:
298:
bends to highly sinuous, densely looping channels. Channel sinuosity results in significant migration lateral and affects continuity of
818:
110:
44:
218:. These cover single channels, a single channel and associated sediments or multiple channels grouped. Flood (2001) defines a
91:
48:
1207:
McHargue, Timothy R. (1991). "Seismic Facies, Processes, and
Evolution of Miocene Inner Fan Channels, Indus Submarine Fan".
63:
317:
There seems to be a potential consensus that truly sinuous channel can be defined as one that displays a minimum average
70:
1180:
Kolla, V.; Coumes, F. (1987). "Morphology, internal structure, seismic stratigraphy, and sedimentation of indus fan".
1069:"Quantitative analysis of the geometry of submarine channels: Implications for the classification of submarine fans"
294:
Sinuosity in submarine channels is a feature regularly observed on seismic maps. It can vary between occasional low
230:
lowstands. A collection of these channels and levees along with overbank sediments form a channel-levee complex.
37:
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as a single channel with a levee at each side. These levees are formed by the overspilling and flow stripping of
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The effect of Earth's rotation causes more sediment to build up on one side of the channel than on the other.
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body forming a constructional wedge of sediment that thins perpendicularly away from a channel-belt. The
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819:"Architecture and evolution of upper fan channel-belts on the Niger Delta slope and in the Arabian Sea"
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There are numerous terms that are used to describe the features contained in this study, including
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582:"3D seismic interpretation of slump complexes: examples from the continental margin of Israel"
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861:"Seismic geomorphology and stratigraphy of depositional elements in deep-water settings"
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They can be V or U in shape, have the presence or lack of depositional margins, highly
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to describe this sinuosity, a phrase used to describe similar sinuosity observed in
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Seismic Facies and
Sedimentary Processes of Submarine Fans and Turbidite Systems
406:
360:
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26:
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Deptuck, Mark E; Steffens, Gary S; Barton, Mark; Pirmez, Carlos (1 June 2003).
1211:. Frontiers in Sedimentary Geology. Springer, New York, NY. pp. 403–413.
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They do, however, remain one of the least understood sedimentary processes.
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1149:. Sinuous Deep-Water Channels: Genesis, Geometry and Architecture.
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Channels in the sea floor formed by fast-flowing turbidity currents
774:. Thematic set on strategic evolution of deep-water architecture.
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Frey
Martinez, Jose; Cartwright, Joe; Hall, Ben (1 March 2005).
1243:. Consortium for Ocean Leadership. 23 May 2014. Archived from
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Clark, J. D.; Kenyon, N. H.; Pickering, K. T. (1 July 1992).
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10.1130/0091-7613(1992)020<0633:QAOTGO>2.3.CO;2
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Schwarz, Ernesto; Arnott, R. William C. (1 February 2007).
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Posamentier, Henry W.; Kolla, Venkatarathnan (1 May 2003).
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carried by the water causing a build-up of the surrounding
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10.1130/0016-7606(1987)98<728:QCOSDC>2.0.CO;2
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this, PJeff
Peakall advocates the avoidance of the term
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List of landforms § Coastal and oceanic landforms
1241:"Underwater Waves are the Earth's 'Lumbering Giants'"
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The morphology and topography of the slope that any
51:. Unsourced material may be challenged and removed.
988:Geological Society, London, Special Publications
766:Kane, Ian A.; Hodgson, David M. (1 March 2011).
185:to the deeper parts of the continental margins.
8:
142:. They are formed by fast-flowing floods of
1046:10.1306/2DC4091C-0E47-11D7-8643000102C1865D
111:Learn how and when to remove this message
245:Ian Kane advocates the use of the terms
226:. These are most likely to occur during
687:"Sea floor geology – Hikurangi Channel"
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161:Submarine channels and their flanking
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49:adding citations to reliable sources
1113:. Turbidites: Models and Problems.
828:. Turbidites: Models and Problems.
691:Te Ara Encyclopedia of New Zealand
195:which take concepts even further.
150:near the channel's head, with the
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257:External levees are a dominantly
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868:Journal of Sedimentary Research
838:10.1016/j.marpetgeo.2003.01.004
784:10.1016/j.marpetgeo.2010.05.009
745:10.1016/j.marpetgeo.2006.08.001
635:Journal of Sedimentary Research
559:10.1016/j.marpetgeo.2008.09.011
512:Journal of Sedimentary Research
290:Channel sinuosity and migration
216:confined channel complex system
36:needs additional citations for
393:Underwater channels can carry
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1000:10.1144/GSL.SP.2004.222.01.06
338:controls such; shape channel
241:Architecture and nomenclature
1217:10.1007/978-1-4684-8276-8_22
1147:Marine and Petroleum Geology
1111:Marine and Petroleum Geology
826:Marine and Petroleum Geology
772:Marine and Petroleum Geology
733:Marine and Petroleum Geology
547:Marine and Petroleum Geology
165:are commonly referred to as
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171:geomorphological features
385:or subsurface folding.
169:. They are significant
345:Lateral migration and
167:channel levee systems
1247:on 11 September 2017
937:10.2110/jsr.2007.015
880:10.1306/111302730367
524:10.2110/jsr.2010.003
220:channel-levee system
45:improve this article
667:Masson et al., 2006
647:10.2110/jsr.2006.02
460:Weimer et al., 2000
212:channel complex set
132:underwater channels
905:on 2 January 2020.
676:Shipp et al., 2004
224:turbidity currents
1226:978-1-4684-8278-2
712:Wynn et al., 2007
442:Turbidity current
378:turbidite channel
274:the channel-belt
183:continental shelf
128:deep-sea channels
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1251:10 September
1249:. Retrieved
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43:Please help
38:verification
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332:topographic
309:terrestrial
268:levee crest
138:in Earth's
696:2008-04-09
448:References
432:Sea canyon
305:meandering
148:avalanches
146:caused by
71:newspapers
1194:0149-1423
1167:0264-8172
1131:0264-8172
1093:0091-7613
1054:1527-1404
1016:128603620
1008:0305-8719
973:0149-1423
945:1527-1404
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846:0264-8172
792:0264-8172
753:0264-8172
655:1527-1404
617:130270471
609:1365-2117
567:0264-8172
532:1527-1404
492:0016-7606
427:Sea basin
422:Sea mount
383:diapirism
347:accretion
319:sinuosity
314:systems.
296:amplitude
228:sea level
181:from the
140:sea floor
1267:Category
896:34598056
401:See also
280:thalwegs
200:geo-body
152:sediment
136:channels
1073:Geology
356:thalweg
312:fluvial
284:canyons
235:sinuous
126:(also,
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300:facies
214:, and
179:carbon
163:levees
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1012:S2CID
921:(PDF)
903:(PDF)
892:S2CID
864:(PDF)
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613:S2CID
585:(PDF)
92:JSTOR
78:books
1253:2017
1221:ISBN
1190:ISSN
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528:ISSN
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334:and
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64:news
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