Editing Oceanic trench (section)

=== Erosive versus accretionary margins ===
Convergent margins are classified as erosive or accretionary, and this has a strong influence on the morphology of the inner slope of the trench. Erosive margins, such as the northern Peru-Chile, Tonga-Kermadec, and Mariana trenches, correspond to sediment-starved trenches.{{sfn|Kearey|Klepeis|Vine|2009|p=250}} The subducting slab erodes material from the lower part of the overriding slab, reducing its volume. The edge of the slab experiences subsidence and steepening, with normal faulting. The slope is underlain by relative strong igneous and metamorphic rock, which maintains a high angle of repose.{{sfn|Geersen|Voelker|Behrmann|2018|p=416}} Over half of all convergent margins are erosive margins.{{sfn|Stern|2005}}

Accretionary margins, such as the southern Peru-Chile, Cascadia, and Aleutians, are associated with moderately to heavily sedimented trenches. As the slab subducts, sediments are "bulldozed" onto the edge of the overriding plate, producing an ''[[accretionary wedge]]'' or ''accretionary prism''. This builds the overriding plate outwards. Because the sediments lack strength, their angle of repose is gentler than the rock making up the inner slope of erosive margin trenches. The inner slope is underlain by [[Imbrication (sedimentology)|imbricated]] [[thrust sheets]] of sediments. The inner slope topography is roughened by localized [[mass wasting]].{{sfn|Geersen|Voelker|Behrmann|2018|p=416}} Cascadia has practically no bathymetric expression of the outer rise and trench, due to complete sediment filling, but the inner trench slope is complex, with many thrust ridges. These compete with canyon formation by rivers draining into the trench.  Inner trench slopes of erosive margins rarely show thrust ridges.{{sfn|Geersen|Voelker|Behrmann|2018|p=420}}

Accretionary prisms grow in two ways. The first is by frontal accretion, in which sediments are scraped off the downgoing plate and emplaced at the front of the accretionary prism.{{sfn|Stern|2005}} As the accretionary wedge grows, older sediments further from the trench become increasingly [[lithification|lithified]], and faults and other structural features are steepened by rotation towards the trench.{{sfn|Kearey|Klepeis|Vine|2009|pp=264–266}} The other mechanism for accretionary prism growth is underplating<!-- not the same as magmatic underplating!-->{{sfn|Stern|2005}} (also known as basal accretion{{sfn|Bangs|Morgan|Tréhu|Contreras-Reyes|2020}}) of subducted sediments, together with some [[oceanic crust]], along the shallow parts of the subduction decollement. The [[Franciscan Group]] of [[California]] is interpreted as an ancient accretionary prism in which underplating is recorded as tectonic mélanges and duplex structures.{{sfn|Stern|2005}}

[[File:Oceanic-oceanic convergence Fig21oceanocean.gif|thumb|upright=1.1|Oceanic trench formed along an oceanic-oceanic [[convergent boundary]]]]
[[File:Cross section of mariana trench.svg|right|upright=1.7|thumb| The [[Mariana Trench]] contains the deepest part of the world's oceans, and runs along an oceanic-oceanic convergent boundary. It is the result of the oceanic [[Pacific plate]] [[subduction|subducting]] beneath the oceanic [[Mariana plate]].]]