Continental Rifted Margins 1. Gwenn Peron-Pinvidic
Чтение книги онлайн.
Читать онлайн книгу Continental Rifted Margins 1 - Gwenn Peron-Pinvidic страница 17
Название: Continental Rifted Margins 1
Автор: Gwenn Peron-Pinvidic
Издательство: John Wiley & Sons Limited
Жанр: Физика
isbn: 9781119986911
isbn:
In structural geology, boudinage refers to a deformed structure produced during the extension of a rock that is characterized by the presence of sheared rigid parts enclosed in a less competent surrounding matrix (Figure 1.23). The “boudins” correspond to pieces of the more rigid rocks that were once part of a continuous layer and have been broken into individual units, isolated laterally by anastomosing shear zones deformed in the ductile or semi-ductile stress-field. Some boudins exhibit a “pinch-and-swell” geometry. Boudinage structures can occur at all scales from microscopic to lithospheric. In rifted margin studies, it has been proposed that the continental lithosphere may deform at the regional scale under such a deformation mode. It is usually associated with specific geological settings including high thermal conditions.
Figure 1.22. Schematic illustration of the evolution of low-angle normal faults (LANFs) with the domino-block rotation model and the rolling-hinge model (source: modified from Ricketts et al. 2015)
1.3.2.6. Folds
Folds can occur at various geologic scales and in various tectonic settings. Intuitively, folds are often associated with shortening rather than extension. However, they may also develop in extensional settings in specific structural contexts, such as in fault propagation folds (folding above a fault tip) or related to the intrusion of igneous material (e.g. above a laccolith). They can also be associated with differential compaction of sedimentary layers. Constrictional strain can also produce folds and compressional geometries in basins under regional extension (e.g. SW Norway Devonian basins, Osmundsen Andersen 2001). Folds are analyzed based on their overall geometry. The three main categories of folds are monocline, anticline and syncline. Geometrically, they are described by how the limbs dip to the hinge axis (Figure 1.24).
Figure 1.23. a) Illustration of a schematic boudinage structure; b) field examples of “pinch-and-swell” boudins from Norway with amphibolite boudins within quartz schists (top: Finnmark, Norway) and a deformed pegmatite dike (bottom: Roan, Norway) (photo credits © Steffen Bergh and © Haakon Fossen) and c) an offshore seismic reflection example from the Gabon rifted margin (source: modified from Clerc et al. 2018)
Figure 1.24. a) Illustration of the main fold geometries; b) field example photos from Portugal (photo credits © Haakon Fossen) and c) seismic refection profile examples of fault-propagation folds associated with different sets of “simple” and “conjugate” normal faults, from the Inner Moray Firth, UK (source: from Lapadat et al. 2017)
Further reading.– The above descriptions are abbreviated and often simplified. If interested in reading and learning further, the reader is referred to the following list of publications and references:
– General: (Wernicke 1985; Lister et al. 1986; Buck 1988, 1991; Lavier et al. 1999; Axen 2004; Davis and Kusznir 2004; Reston 2007, 2009; Reston and McDermott 2011; Whitney et al. 2014; Jackson et al. 2017; Brun et al. 2018; Rotevatn et al. 2019).
– For structural geology definitions, we recommend the excellent book (Fossen 2010).
1.3.3. Main basin types
Rifts and rifted margins are usually composed of several basins of various types and linked in various ways. Below is a list of the major types of basins that can be encountered in rift and rifted margin studies. Again, this list does not aim at being entirely complete, but representative of the main geometries encountered in rifts and rifted margins.
1.3.3.1. Grabens, half-grabens and horsts
Grabens and half-grabens are the most common type of sedimentary basins generated in extensional settings. A graben is typically identified as a valley flanked by distinct topographic escarpments. Structurally, grabens are formed by arrays of oppositely dipping normal faults. In the ideal case, the flanking faults are parallel and antithetic and grow at the same rate so that there is no rotation of the hanging wall. The overall downward movement of the common hanging wall leads to the formation of a symmetric depression: the graben (Figure 1.25). However, faults rarely grow at the same rate, so grabens are usually asymmetric. If several faults form, the hanging wall platform can be further dissected and can generate a horst (Figure 1.25). Half-grabens correspond to the topographic depression developed on the tilted hanging walls of normal faults.
Figure 1.25. Diagram illustrating the structural geometries of a graben, horst and half-graben
1.3.3.2. Pull-apart basins
In some cases, extension can occur related to strike-slip faults. In regions with multiple segments of strike-slip faults, the lateral displacement between the faults will lead to stepovers and, eventually, the development of pull-apart basins – also named strike-slip basins (Figure 1.26). Typically, pull-apart basins are strongly compartmentalized, with each individual basin sharing similarities with discrete intracontinental rifts. The standard basin geometry corresponds to a rhomb-shaped graben or half-graben. In theory, these basins tend to be fairly deep with a fast subsidence. Type examples of strike-slip faults with pull-apart basins include the San Andreas Fault, the Dead Sea Transform and the North Anatolian Fault (Şengör et al. 2005). The most cited examples of strike-slip rifts include the Salton Sea, the Death Valley, the Jordan Valley-Dead Sea Rift – Gulf of Eilat and the onshore northernmost part of the Red Sea Rift.
Figure 1.26. Diagram illustrating the main structural geometries associated with a pull-apart basin, at its early stage of development (source: modified from Wu et al. 2009, based on analogue modeling results)
1.3.3.3. Sag basins
In geology, the term “sag СКАЧАТЬ