Mountain formation refers to the geological processes that underlie the formation of mountains. These processes are associated with large-scale movements of the Earth's crust (tectonic plates). Folding, faulting, volcanic activity, igneous intrusion and metamorphism can all be parts of the orogenic process of mountain building. The formation of mountains is not necessarily related to the geological structures found on it.
The understanding of specific landscape features in terms of the underlying tectonic processes is called tectonic geomorphology, and the study of geologically young or ongoing processes is called neotectonics.[clarification needed]
Types of mountains
There are four main types of mountains: volcanic, fold,residual, and block. A more detailed classification useful on a local scale predates plate tectonics and adds to these categories.
Movements of tectonic plates create volcanoes along the plate boundaries, which erupt and form mountains. A volcanic arc system is a series of volcanoes that form near a subduction zone where the crust of a sinking oceanic plate melts and drags water down with the subducting crust.
Most volcanoes occur in a band encircling the Pacific Ocean (the Pacific Ring of Fire), and in another that extends from the Mediterranean across Asia to join the Pacific band in the Indonesian Archipelago. The most important types of volcanic mountain are composite cones or stratovolcanoes (Vesuvius, Kilimanjaro and Mount Fuji are examples) and shield volcanoes (such as Mauna Loa on Hawaii, a hotspot volcano).
A shield volcano has a gently sloping cone due to the low viscosity of the emitted material, primarily basalt. Mauna Loa is the classic example, with a slope of 4°-6°. (The relation between slope and viscosity falls under the topic of angle of repose.) The composite volcano or stratovolcano has a more steeply rising cone (33°-40°), due to the higher viscosity of the emitted material, and eruptions are more violent and less frequent than for shield volcanoes. Besides the examples already mentioned are Mount Shasta, Mount Hood and Mount Rainier. Vitosha - the domed mountain next to Sofia, capital of Bulgaria, is also formed by volcanic activity.
When plates collide or undergo subduction (that is – ride one over another), the plates tend to buckle and fold, forming mountains. Most of the major continental mountain ranges are associated with thrusting and folding or orogenesis. Examples are the Balkan Mountains, the Jura and the Zagros mountains.
When a fault block is raised or tilted, block mountains can result. Higher blocks are called horsts and troughs are called grabens. A spreading apart of the surface causes tensional forces. When the tensional forces are strong enough to cause a plate to split apart, it does so such that a center block drops down relative to its flanking blocks.
An example of this is the Sierra Nevada Range, where delamination created a block 650 km long and 80 km wide that consists of many individual portions tipped gently west, with east facing slips rising abruptly to produce the highest mountain front in the continental United States.
Another good example is the Rila - Rhodope mountain Massif in Bulgaria, Southeast Europe, including the well defined horsts of Belasitsa (linear horst), Rila mountain (vaulted domed shaped horst) and Pirin mountain - a horst forming a massive anticline situated between the complex graben valleys of Struma and that of Mesta.
Uplifted passive margins
Unlike orogenic mountains there is no widely accepted geophysical model that explains elevated passive continental margins such as the Scandinavian Mountains, Eastern Greenland, the Brazilian Highlands or Australia's Great Dividing Range. Different elevated passive continental margins most likely share the same mechanism of uplift. This mechanism is possibly related to far-field stresses in Earth's lithosphere. According to this view elevated passived margins can be likened to giant anticlinal lithospheric folds, where folding is caused by horizontal compression acting on a thin to thick crust transition zone (as are all passive margins).
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Residual mountains are formed as a result of erosion of an existing elevated area. They are also called mountains of denudation.
Examples in Europe include: the Eastern Rhodopes, part of the Rila-Rhodope mountain massif, which is the oldest landmass on the Balkan Peninsula, the Scottish Highlands, the Scandinavian Mountains, and Snowdonia in Wales.
Hotspots are supplied by a magma source in the Earth's mantle called a mantle plume. Although originally attributed to a melting of subducted oceanic crust, recent evidence belies this connection. The mechanism for plume formation remains a research topic.
Several movements of the earth's crust that lead to mountains are associated with faults. These movements actually are amenable to analysis that can predict, for example, the height of a raised block and the width of an intervening rift between blocks using the rheology of the layers and the forces of isostasy. Early bent plate models predicting fractures and fault movements have evolved into today's kinematic and flexural models.
- 3D fold evolution
- Continental collision
- Cycle of erosion
- Inselberg – Isolated rock hill or small mountain that rises abruptly from a relatively flat surrounding plain
- Orogeny – The formation of mountain ranges
- Tectonics – The processes that control the structure and properties of the Earth's crust and its evolution through time
- Seamount – A mountain rising from the ocean seafloor that does not reach to the water's surface
- Steven M. Stanley (2004). "Mountain building". Earth system history (2nd ed.). Macmillan. p. 207. ISBN 0-7167-3907-0.
- Robert J. Twiss; Eldridge M. Moores (1992). "Plate tectonic models of orogenic core zones". Structural Geology (2nd ed.). Macmillan. p. 493. ISBN 0-7167-2252-6.
- Ollier, Cliff; Pain, Colin (2000). The Origin of Mountains. Routledge. p. 1. ISBN 0-415-19890-9.
- Kurt Stüwe (2007). "§4.5 Geomorphology". Geodynamics of the lithosphere: an introduction (2nd ed.). Springer. p. 178. ISBN 3-540-71236-4.
- "Geosynclinal Theory". publish.illinois.edu. University of Illinois at Urbana-Champaign. Retrieved March 8, 2018.
The major mountain-building idea that was supported from the 19th century and into the 20th is the geosynclinal theory.
- Andrew Goudie (2004). Encyclopedia of geomorphology; Volume 2. Routledge. p. 701. ISBN 0-415-32738-5.
- NASA - Activity at Kliuchevskoi
- Victor Schmidt; William Harbert (2003). Planet Earth and the New Geoscience (4th ed.). Kendall Hunt. pp. 46–47. ISBN 0-7872-9355-5.
- Stephen D Butz (2004). "Chapter 8: Plate tectonics". Science of Earth Systems. Thompson/Delmar Learning. p. 136. ISBN 0-7668-3391-7.
- John Gerrard (1990). "Types of volcano". Mountain environments: an examination of the physical geography of mountains. MIT Press. p. 194. ISBN 0-262-07128-2.
- Robert Wayne Decker; Barbara Decker (2005). "Chapter 8: Hot spots". Volcanoes (4th ed.). Macmillan. p. 113 ff. ISBN 0-7167-8929-9.
- Arthur Holmes; Donald Duff (2004). Holmes Principles of Physical Geology (4th ed.). Taylor & Francis. p. 209. ISBN 0-7487-4381-2.
- Transactions of the American Society of Civil Engineers, Volume 39. American Society of Civil Engineers. 1898. p. 62.
- James Shipman; Jerry D. Wilson; Aaron Todd (2007). "Minerals, rocks and volcanoes". An Introduction to Physical Science (12th ed.). Cengage Learning. p. 650. ISBN 0-618-93596-7.
- Michael P Searle (2007). "Diagnostic features and processes in the construction and evolution of Oman-, Zagros-, Himalayan-, Karakoram-, and Tibetan type orogenic belts". In Robert D Hatcher Jr.; MP Carlson; JH McBride & JR Martinez Catalán. 4-D framework of continental crust. Geological Society of America. p. 41 ff. ISBN 0-8137-1200-9.
- Chris C. Park (2001). "Figure 6.11". The environment: principles and applications (2nd ed.). Routledge. p. 160. ISBN 0-415-21770-9.
- Scott Ryan (2006). "Figure 13-1". CliffsQuickReview Earth Science. Wiley. ISBN 0-471-78937-2.
- John Gerrard (1990-04-12). Reference cited. p. 9. ISBN 0-262-07128-2.
- Lee, C.-T.; Yin, Q; Rudnick, RL; Chesley, JT; Jacobsen, SB (2000). "Osmium Isotopic Evidence for Mesozoic Removal of Lithospheric Mantle Beneath the Sierra Nevada, California" (PDF). Science. 289 (5486): 1912–6. Bibcode:2000Sci...289.1912L. doi:10.1126/science.289.5486.1912. PMID 10988067. Archived from the original (PDF) on 2011-06-15.
- Geographic Dictionary of Bulgaria 1980, p. 368
- Dimitrova & al 2004, p. 53
- Donchev & Karakashev 2004, pp. 128–129
- Bonow, Johan M. (2009). "atlantens kustberg och högslätter – gamla eller unga?" (PDF). www.geografitorget.se (in Swedish). Geografilärarnas Riksförening.
- Green, Paul F.; Lidmar-Bergström, Karna; Japsen, Peter; Bonow, Johan M.; Chalmers, James A. (2013). "Stratigraphic landscape analysis, thermochronology and the episodic development of elevated, passive continental margins". Geological Survey of Denmark and Greenland Bulletin. 30: 18. Archived from the original on 24 September 2015. Retrieved 30 April 2015.
- Japsen, Peter; Chalmers, James A.; Green, Paul F.; Bonow, Johan M. (2012). "Elevated, passive continental margins: Not rift shoulders, but expressions of episodic, post-rift burial and exhumation". Global and Planetary Change. 90-91: 73–86. Bibcode:2012GPC....90...73J. doi:10.1016/j.gloplacha.2011.05.004.
- Løseth and Hendriksen 2005
- The Rilo-Rhodope massif is sometimes referred to as the Rhodope mountains alone.
- Y Niu & MJ O'Hara (2004). "Chapter 7: Mantle plumes are NOT from ancient oceanic crust". In Roger Hékinian; Peter Stoffers & Jean-Louis Cheminée. Oceanic hotspots: intraplate submarine magmatism and tectonism. Springer. p. 239 ff. ISBN 3-540-40859-2.
- AB Watts (2001). "§7.2 Extensional tectonics and rifting". Isostasy and flexure of the lithosphere. Cambridge University Press. p. 295. ISBN 0-521-00600-7.
- GD Karner & NW Driscoll (1999). "Style, timing and distribution of tectonic deformation across the Exmouth Plateau, northwest Australia, determined from stratal architecture and quantitative basin modelling". In Conall Mac Niocaill & Paul Desmond Ryan. Continental tectonics. Geological society. p. 280. ISBN 1-86239-051-7.