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Geologic provinces of the world (USGS)
  Extended crust
Oceanic crust:
  0–20 Ma
  20–65 Ma
  >65 Ma

Orogeny refers to forces and events leading to a large structural deformation of the Earth's lithosphere (crust and uppermost mantle) due to the engagement of tectonic plates. Response to such engagement results in the formation of long tracts of highly deformed rock called orogens or orogenic belts. The word "orogeny" comes from the Greek (oros for "mountain" plus genesis for "creation" or "origin"),[1] and it is the primary mechanism by which mountains are built on continents. Orogens develop while a continental plate is crumpled and is pushed upwards to form mountain ranges, and involve a great range of geological processes collectively called orogenesis.[2][3]


Two processes that can contribute to an orogen. Top: delamination by intrusion of hot asthenosphere; Bottom: Subduction of ocean crust. The two processes lead to differently located granites (bubbles in diagram), providing evidence as to which process actually occurred.[4]
Subduction of an oceanic plate by a continental plate to form a noncollisional orogen. (example: the Andes)
Continental collision of two continental plates to form a collisional orogen. However, usually no continental crust is subducted, only uplifted. (example: the Alps)

Formation of an orogen is accomplished in part by the tectonic processes of subduction, where a continent rides forcefully over an oceanic plate (noncollisional orogens), or convergence of two or more continents (collisional orogens).[5]

Orogeny usually produces long arcuate (from arcuare, to bend like a bow) structures, known as orogenic belts. Generally, orogenic belts consist of long parallel strips of rock exhibiting similar characteristics along the length of the belt. Orogenic belts are associated with subduction zones, which consume crust, produce volcanoes, and build island arcs. The arcuate structure is attributed to the rigidity of the descending plate, and island arc cusps are related to tears in the descending lithosphere.[6] These island arcs may be added to a continent during an orogenic event.

The processes of orogeny can take tens of millions of years and build mountains from plains or the ocean floor. The topographic height of orogenic mountains is related to the principle of isostasy,[7] that is, a balance of the downward gravitational force upon an upthrust mountain range (composed of light, continental crust material) and the buoyant upward forces exerted by the dense underlying mantle.[8]

Frequently, rock formations that undergo orogeny are severely deformed and undergo metamorphism. During orogeny, deeply buried rocks may be pushed to the surface. Sea bottom and near shore material may cover some or all of the orogenic area. If the orogeny is due to two continents colliding, the resulting mountains can be very high (see Himalaya).

An orogenic event may be studied as: (a) a tectonic structural event, (b) as a geographical event, and (c) a chronological event. Orogenic events: (a) cause distinctive structural phenomena related to tectonic activity, (b) affect rocks and crust in particular regions, and (c) happen within a specific period.

Orogenic system[edit]

An orogeny produces an orogenic system, or (mountain) range-foredeep-foreland system.

The foredeep is the subsidence zone ahead the mountain range toward the subsident plate which the pushed rocks strata of the mountain range converge toward; there post-orogenic sediments from the erosion of the rocks of the mountain range lifting up (molassic sediments) flow.

The foreland is the zone ahead the foredeep, either of the geological succession, or of the lateral transition of that, of the foredeep basement which molassic sediments flow on.

Orogenic cycle[edit]

Although orogeny involves plate tectonics, the tectonic forces result in a variety of associated phenomena, including magmatization, metamorphism, crustal melting, and crustal thickening. Just what happens in a specific orogen depends upon the strength and rheology of the continental lithosphere, and how these properties change during orogenesis.

In addition to orogeny, the orogen once formed is subject to other processes, such as sedimentation and erosion.[3] The sequence of repeated cycles of sedimentation, deposition and erosion, followed by burial and metamorphism, and then by formation of granitic batholiths and tectonic uplift to form mountain chains, is called the orogenic cycle.[9][10] For example, the Caledonian Orogeny refers to the Silurian and Devonian events that resulted from the collision of Laurentia with Eastern Avalonia and other former fragments of Gondwana. The Caledonian Orogen resulted from these events and various others that are part of its peculiar orogenic cycle.[11]

In summary, an orogeny is a long-lived deformational episode during which many geological phenomena play a role. The orogeny of an orogen is only part of the orogen's orogenic cycle.


Erosion is a subsequent phase of the orogenic cycle. Erosion inevitably removes much of the mountains, exposing the core or mountain roots (metamorphic rocks brought to the surface from a depth of several kilometres). Such exhumation may be helped by isostatic movements balancing out the buoyancy of the evolving orogen. Debate exists about the extent to which erosion modifies the patterns of tectonic deformation (see erosion and tectonics). Thus, the final form of the majority of old orogenic belts is a long arcuate strip of crystalline metamorphic rocks sequentially below younger sediments which are thrust atop them and dip away from the orogenic core.

An orogen may be almost completely eroded away, and only recognizable by studying (old) rocks that bear traces of orogenesis. Orogens are usually long, thin, arcuate tracts of rock that have a pronounced linear structure resulting in terranes or blocks of deformed rocks, separated generally by suture zones or dipping thrust faults. These thrust faults carry relatively thin slices of rock (which are called nappes or thrust sheets, and differ from tectonic plates) from the core of the shortening orogen out toward the margins, and are intimately associated with folds and the development of metamorphism.[12]


The study of orogeny, coupled with biogeography (the study of the distribution and evolution of flora and fauna),[13] geography and mid ocean ridges in the 1950s and 1960s, contributed greatly to the theory of plate tectonics. Even at a very early stage, life played a significant role in the continued existence of oceans, by affecting the composition of the atmosphere. The existence of oceans is critical to sea-floor spreading and subduction.[14][15]

Relationship to mountain building[edit]

An example of thin-skinned deformation (thrust faulting) of the Sevier Orogeny in Montana. Note the white Madison Limestone repeated, with one example in the foreground (that pinches out with distance) and another to the upper right corner and top of the picture.
Sierra Nevada Mountains (a result of delamination) as seen from the International Space Station.

Mountain formation occurs through a number of mechanisms.[16][17][18]

Mountain complexes result from irregular successions of tectonic responses due to sea-floor spreading, shifting lithosphere plates, transform faults, and colliding, coupled and uncoupled continental margins.


Large modern orogenies often lie on the margins of continents; the Alleghenian (Appalachian), Laramide, and Andean orogenies are examples of these in the Americas. Older inactive orogenies, such as the Algoman, Penokean and Antler, are represented by deformed rocks and sedimentary basins further inland.

Areas that are rifting apart, such as mid-ocean ridges and the East African Rift, have mountains due to thermal buoyancy related to the hot mantle underneath them; this thermal buoyancy is known as dynamic topography. In strike-slip systems, such as the San Andreas Fault, restraining bends result in regions of localized crustal shortening and mountain building without a plate-margin-wide orogeny. Hotspot volcanism results in the formation of isolated mountains and mountain chains that are not necessarily on tectonic plate boundaries.

Regions can also experience uplift as a result of delamination of the lithosphere, in which an unstable portion of cold lithospheric root drips down into the mantle, decreasing the density of the lithosphere and causing buoyant uplift.[20] An example is the Sierra Nevada in California. This range of fault-block mountains[21] experienced renewed uplift after a delamination of the lithosphere beneath them.[20][22]

Finally, uplift and erosion related to epeirogenesis (large-scale vertical motions of portions of continents without much associated folding, metamorphism, or deformation)[23] can create local topographic highs.

History of the concept[edit]

Before the development of geologic concepts during the 19th century, the presence of mountains was explained in Christian contexts[citation needed] as a result of the Biblical Deluge. This was an extension of Neoplatonic thought, which influenced early Christian writers[citation needed].

Orogeny was used by Amanz Gressly (1840) and Jules Thurmann (1854) as orogenic in terms of the creation of mountain elevations, as the term mountain building was still used to describe the processes.

Elie de Beaumont (1852) used the evocative "Jaws of a Vise" theory to explain orogeny, but was more concerned with the height rather than the implicit structures created by and contained in orogenic belts. His theory essentially held that mountains were created by the squeezing of certain rocks.

Eduard Suess (1875) recognised the importance of horizontal movement of rocks. The concept of a precursor geosyncline or initial downward warping of the solid earth (Hall, 1859) prompted James Dwight Dana (1873) to include the concept of compression in the theories surrounding mountain-building. With hindsight, we can discount Dana's conjecture that this contraction was due to the cooling of the Earth (aka the cooling Earth theory).

The cooling Earth theory was the chief paradigm for most geologists until the 1960s. It was, in the context of orogeny, fiercely contested by proponents of vertical movements in the crust (similar to tephrotectonics), or convection within the asthenosphere or mantle.

Gustav Steinmann (1906) recognised different classes of orogenic belts, including the Alpine type orogenic belt, typified by a flysch and molasse geometry to the sediments; ophiolite sequences, tholeiitic basalts, and a nappe style fold structure.

In terms of recognising orogeny as an event, Leopold von Buch (1855) recognised that orogenies could be placed in time by bracketing between the youngest deformed rock and the oldest undeformed rock, a principle which is still in use today, though commonly investigated by geochronology using radiometric dating.

H.J. Zwart (1967)[24] drew attention to the metamorphic differences in orogenic belts, proposing three types, modified by W. S. Pitcher in 1979[25] and further modified as:[citation needed]

The advent of plate tectonics has explained the vast majority of orogenic belts and their features. The cooling earth theory (principally advanced by Descartes) is dispensed with, and tephrotectonic style vertical movements have been explained primarily by the process of isostasy.

Some oddities exist, where simple collisional tectonics are modified in a transform plate boundary, such as in New Zealand, or where island arc orogenies, for instance in New Guinea occur away from a continental backstop. Further complications such as Proterozoic continent-continent collisional orogens, explicitly the Musgrave Block in Australia, previously inexplicable (see Dennis, 1982) are being brought to light with the advent of seismic imaging techniques which can resolve the deep crust structure of orogenic belts.

See also[edit]


  1. ^ Chambers 21st Century Dictionary. Allied Publishers. 1999. p. 972. ISBN 978-0550106254. Retrieved 27 June 2012. 
  2. ^ Tony Waltham (2009). Foundations of Engineering Geology (3rd ed.). Taylor & Francis. p. 20. ISBN 0-415-46959-7. 
  3. ^ a b Philip Kearey, Keith A. Klepeis, Frederick J. Vine (2009). "Chapter 10: Orogenic belts". Global Tectonics (3rd ed.). Wiley-Blackwell. p. 287. ISBN 1-4051-0777-4. 
  4. ^ N. H. Woodcock, Robin A. Strachan (2000). "Chapter 12: The Caledonian Orogeny: a multiple plate collision". Geological History of Britain and Ireland. Wiley-Blackwell. p. 202, Figure 12.11. ISBN 0-632-03656-7. 
  5. ^ Frank Press (2003). Understanding Earth (4th ed.). Macmillan. pp. 468–469. ISBN 0-7167-9617-1. 
  6. ^ Gerald Schubert, Donald Lawson Turcotte, Peter Olson (2001). "§2.5.4 Why are island arcs arcs?". Mantle Convection in the Earth and Planets. Cambridge University Press. pp. 35–36. ISBN 0-521-79836-1. 
  7. ^ PA Allen (1997). "Isostasy in zones of convergence". Earth Surface Processes. Wiley-Blackwell. p. 36 ff. ISBN 0-632-03507-2. 
  8. ^ Gerard V. Middleton, Peter R. Wilcock (1994). "§5.5 Isostasy". Mechanics in the Earth and Environmental Sciences (2nd ed.). Cambridge University Press. p. 170. ISBN 0-521-44669-4. 
  9. ^ David Johnson (2004). "The orogenic cycle". The geology of Australia. Cambridge University Press. p. 48 ff. ISBN 0-521-84121-6. 
  10. ^ In other words, orogeny is only a phase in the life of an orogen. Five characteristics of the orogenic cycle are listed by 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. 
  11. ^ N. H. Woodcock, Robin A. Strachan (2000). "Chapter 12: The Caledonian Orogeny: A Multiple Plate Collision". cited work. p. 187 ff. ISBN 0-632-03656-7. 
  12. ^ Olivier Merle (1998). "§1.1 Nappes, overthrusts and fold-nappes". Emplacement Mechanisms of Nappes and Thrust Sheets. Petrology and Structural Geology 9. Springer. p. 1 ff. ISBN 0-7923-4879-6. 
  13. ^ For example, see Patrick L Osborne (2000). Tropical Ecosystems and Ecological Concepts. Cambridge University Press. p. 11. ISBN 0-521-64523-9. "Continental drift and plate tectonics help to explain both the similarities and the differences in the distribution of plants and animals over the continents"  and John C Briggs (1987). Biogeography and Plate Tectonics. Elsevier. p. 131. ISBN 0-444-42743-0. "It will not be possible to construct a thorough account of the history of the southern hemisphere without the evidence from both the biological and the earth sciences" 
  14. ^ Paul D. Lowman (2002). "Chapter 7: Geology and biology: the influence of life on terrestrial geology". Exploring Space, Exploring Earth: New Understanding of the Earth from Space Research. Cambridge University Press. pp. 286–287. ISBN 0-521-89062-4. 
  15. ^ Seema Sharma (2005). "Atmosphere: origin". Encyclopaedia of Climatology. Anmol Publications PVT. LTD. p. 30 ff. ISBN 81-261-2442-3. 
  16. ^ Richard J. Huggett (2007). Fundamentals of Geomorphology (2nd ed.). Routledge. p. 104. ISBN 0-415-39084-2. 
  17. ^ Gerhard Einsele (2000). Sedimentary Basins: Evolution, Facies, and Sediment Budget (2nd ed.). Springer. p. 453. ISBN 3-540-66193-X. "Without denudation, even relatively low uplift rates as characteristic of epeirogenetic movements (e.g. 20m/MA) would generate highly elevated regions in geological time periods." 
  18. ^ Ian Douglas, Richard John Huggett, Mike Robinson (2002). Companion Encyclopedia of Geography: The Environment and Humankind. Taylor & Francis. p. 33. ISBN 0-415-27750-7. 
  19. ^ Peter J Coney (1970). "The Geotectonic Cycle and the New Global Tectonics". Geological Society of America Bulletin 81 (3): 739–748. Bibcode:1970GSAB...81..739C. doi:10.1130/0016-7606(1970)81[739:TGCATN]2.0.CO;2. 
  20. ^ a b 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". Science 289 (5486): 1912–6. Bibcode:2000Sci...289.1912L. doi:10.1126/science.289.5486.1912. PMID 10988067. 
  21. ^ John Gerrard (1990). Mountain Environments: An Examination of the Physical Geography of Mountains. MIT Press. p. 9. ISBN 0-262-07128-2. 
  22. ^ Manley, Curtis R.; Glazner, Allen F.; Farmer, G. Lang (2000). "Timing of Volcanism in the Sierra Nevada of California: Evidence for Pliocene Delamination of the Batholithic Root?". Geology 28 (9): 811. Bibcode:2000Geo....28..811M. doi:10.1130/0091-7613(2000)28<811:TOVITS>2.0.CO;2. 
  23. ^ Arthur Holmes, Doris L. Holmes (2004). Holmes Principles of Physical Geology (4th ed.). Taylor & Francis. p. 92. ISBN 0-7487-4381-2. 
  24. ^ Zwart, H. J., 1967. The duality of orogenicb elts. Geol. Mijnbouw. 46, 283-309 (referred in Pitcher 1979)
  25. ^ W.S. Pitcher, "The nature, ascent and emplacement of granitic magmas", Journal of the Geological Society 1979; v. 136; p. 627-662


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