Thick-skinned deformation is a geological term which refers to crustal shortening that involves basement rocks and deep-seated faults as opposed to only the upper units of cover rocks above the basement which is known as thin-skinned deformation. While thin-skinned deformation is common in many different localities, thick-skinned deformation requires much more strain to occur and is a rarer type of deformation.
Deformation in geology refers to any alterations to the size or shape of a rock formation since the time of its creation. There are many different ways deformation can occur but it is always the result of some amount of stress within a formation. This stress leads to the formation of many structures that can either extend or shorten the length of the crust in the area. Some of the most common structures are faults and folds. Thick-skinned deformation is a specific type of deformation that can take the form of either faults or folds. The term thick-skinned specifically applies type of deformation which affects not only the sedimentary and metamorphic cover rocks near the surface but also affects the much deeper crystalline rock of the basement and may extend even deeper into the lower crust. Thin-skinned deformation is the counterpart to thick-skinned deformation and can frequently be found in similar areas. As the term implies, thin-skinned deformation is deformation that only affects the upper layers of the cover rocks and does not continue into the deeper basement. There is also one other term which may be used as an intermediary between these two extremes. The term basement-involved thin-skinned deformation can be applied to deformation that affects the cover rocks and may cut some into the basement then level off before going too deep.
Thick-skinned deformation is most commonly a result of crustal shortening and occurs when the region is undergoing horizontal compression. This frequently occurs in at the sites of continental collisions where orogenesis, or mountain building, is taking place and during which the crust is shortened horizontally and thickened vertically. The massive compressional forces involved in such a collision cause the basement rock and all of the units above it to deform. Deformation occurs in the form of both folds and thrust faults and may form a fold and thrust belt along the collisional zone or as crustal flow.
At convergent plate boundaries two plates move towards each other as one is subducted downwards beneath the other but when the crust of two continents meet at a convergent zone neither one of them will be subducted due to their low density. As the two continents are pushed together by tectonic processes a large amount of stress is put on the rock. Eventually deformation will occur in one or multiple ways in order to relieve the stress.
Folding usually occurs in areas with a very slow strain rate or when the rock being deformed is relatively weak and ductile. As folding occurs the units of rock bend forming anticlines, ridges, and synclines, valleys. While the true thickness of the underlying crust may not be equal to the elevation changes of the resulting mountains and hills, the average crustal thickness is greater than before the deformation occurred. One way in which folding can occur in such a formation is by a small amount of subduction of one plate. One continent may be partially overridden by the other but since the plate is far too light to sink it will uplift the overriding plate creating very large folds that deform the entire crust.
Thrust faults are another common form of deformation to occur in these areas. Faulting is generally the result of greater strain rates and stronger or more brittle rocks. These faults have a high angle and cause thickening by uplifting the rock onto itself. These types of faults are identified by the vertically repeating stratigraphy that they produce. During a collision when the strain reaches the breaking point of the rock a fracture will form in the rock. This fracture cuts across layers of rock to form a ramp which will allow movement to dissipate the accumulated strain. Under compression the upper hanging wall rises and overrides the lower foot wall.
The final type of deformation is crustal flow. This type of deformation is only able to occur when the crustal material is heated to a very high temperature, approximately 2/3 of its melting temperature. When this occurs in a collisional zone then the rock can be deformed by creep and will behave similarly to a fluid over the long periods of geologic time.
- Himalayan Mountains - The Himalayas of Tibet are at the location of a continental collision between the Indian and Asian continents and contains many examples of thick-skinned deformation.
- Andes Mountains - The Andes of South America are at the location of an ancient subduction zone and are formed by thick-skinned deformation.
- Pfiffner, Adrian (2006). "Thick-skinned and thin-skinned styles of continental contraction". Geological Society of America. 414: 153–177. doi:10.1130/2006.2414(09). Retrieved 5 November 2012.
- "Plate Tectonics". Retrieved 2 December 2012.
- Copley, Alex; Dan McKenzie (2007). "Models of crustal ﬂow in the India–Asia collision zone" (PDF). Geophysics (169): 683–698. doi:10.1111/j.1365-246X.2007.03343.x. Retrieved 5 November 2012.
- "Thin- and Thick-Skinned Deformation Associated with Flat Subduction". Retrieved 3 December 2012.