Editing Rift (section)

===Rifting to break-up===
Rifting may lead to continental breakup and formation of oceanic basins. Successful rifting leads to seafloor spreading along a mid-oceanic ridge and a set of conjugate margins separated by an oceanic basin.<ref>{{cite journal|author1=Ziegler P.A. |author2=Cloetingh S.|title=Dynamic processes controlling evolution of rifted basins |journal=Earth-Science Reviews |date=January 2004 |volume=64 |issue=1–2 |pages=1–50 |doi=10.1016/S0012-8252(03)00041-2|bibcode=2004ESRv...64....1Z }}</ref> Rifting may be active, and controlled by [[mantle convection]]. It may also be passive, and driven by far-field tectonic forces that stretch the lithosphere. Margin architecture develops due to spatial and temporal relationships between extensional deformation phases. Margin segmentation eventually leads to the formation of rift domains with variations of the [[Mohorovičić discontinuity|Moho]] topography, including proximal domain with fault-rotated crustal blocks, necking zone with thinning of crustal [[Basement (geology)|basement]], distal domain with deep sag basins, ocean-continent transition and oceanic domain.<ref name="Marine and Petroleum Geology">{{cite journal|author1=Péron-Pinvidic G.|author2=Manatschal G.|author3=Osmundsen P.T.|title=Structural comparison of archetypal Atlantic rifted margins: a review of observations and concepts|journal=Marine and Petroleum Geology|date=May 2013|volume=43 |pages=21–47 |doi=10.1016/j.marpetgeo.2013.02.002|bibcode=2013MarPG..43...21P }}</ref>

Deformation and magmatism interact during rift evolution. Magma-rich and magma-poor rifted margins may be formed.<ref name="Marine and Petroleum Geology"/> Magma-rich margins include major volcanic features. Globally, volcanic margins represent the majority of passive continental margins.<ref>{{cite book|author1=Reston T.J.|author2=Manatschal G.|title=Building blocks of later collision|editor=Brown D. & Ryan P.D.|publisher=Frontiers in Earth Sciences|year=2011|chapter=Arc-Continent Collision}}</ref> Magma-starved rifted margins are affected by large-scale faulting and crustal hyperextension.<ref>{{cite journal|author1=Péron-Pinvidic G.|author2=Manatschal G.|title=The final rifting evolution at deep magma-poor passive margins from Iberia-Newfoundland: a new point of view|journal=International Journal of Earth Sciences|year=2009|volume=98|issue=7 |page=1581 |doi=10.1007/s00531-008-0337-9 |bibcode=2009IJEaS..98.1581P |s2cid=129442856 }}</ref> As a consequence, upper mantle peridotites and gabbros are commonly exposed and serpentinized along extensional detachments at the seafloor.