Rifts and passive margins. Structural architecture, thermal regimes and petroleum systems / Рифты и пассивные окраины. Структурная архитектура, температурные режимы и углеводородные системы

Based on the behavior of the asthenosphere, the rifting is driven by passive and active rifting components (Sengör and Burke, 1978; Figure 1.2), which are understood as rather end-members of the natural rift types driven by the mixture of these components (see, e.g., Huismans, 1999; Davis and Kusznir, 2002; Manatschal, 2004; Huismans and Beaumont, 2005; Simon and Podladchikov, 2006).
Passive rifting is characterized by passive asthenospheric upwelling in response to overlying layers separation controlled by regional tectonic extension (Keen, 1985; Ruppel, 1995; Kincaid et al., 1996). In this case, the lithosphere is thinned only in response to extension. The passive asthenospheric upwelling drives many secondary processes such as decompression-driven melting, crustal/lithospheric magma underplating, eruption of continental flood basalts, the onset of secondary convection, and development of large thermal gradients between extended and unextended regions (e.g., McKenzie and Bickle, 1988; Ruppel, 1995; Huismans et al., 2001). <...>