Orogeny Totally Explained

Everything about Orogeny totally explained

Orogeny (Greek for "mountain generating") is the process of natural mountain building, and may be studied as a tectonic structural event, as a geographical event and a chronological event, in that orogenic events cause distinctive structural phenomena and related tectonic activity, affect certain regions of rocks and crust and happen within a time frame.
   Orogenic events occur solely as a result of the processes of plate tectonics; the problems which were investigated and resolved by the study of orogenesis contributed greatly to the theory of plate tectonics, coupled with study of flora and fauna, geography and mid ocean ridges in the 1950s and 1960s.
   The physical manifestations of orogenesis (the process of orogeny) are orogenic belts or orogens. An orogen is different from a mountain range in that an orogen may be completely eroded away, and only recognizable by studying (old) rocks that bear the traces of the orogeny. Orogens are usually long, thin, arcuate tracts of rocks which have a pronounced linear structure resulting in terranes or blocks of deformed rocks, separated generally by dipping thrust faults. These thrust faults carry relatively thin plates (which are called nappes, and differ from tectonic plates) of rock in from the margins of the compressing orogen to the core, and are intimately associated with folds and the development of metamorphism.
   The topographic height of orogenic mountains is related to the principle of isostasy, where the gravitational force of the upthrust mountain range of light, continental crust material is balanced against its buoyancy relative to the dense mantle. Erosion inevitably takes its course, removing much of the mountains and exposing the core or mountain roots (metamorphic rocks brought from tens of km depth to the surface). Such exhumation may be helped by isostatic movements balancing out the buoyancy of the evolving orogen. It is a question of debate to what extent can erosion modify the patterns of tectonic deformacion (see erosion and tectonics). This is the final form of the majority of old orogenic belts, being a long arcuate strip of crystalline metamorphic rocks sequentially below younger sediments which are thrust atop them and dip away from the orogenic core.

History

Before the development of geologic concepts during the 19th century, the presence of mountains was explained in Christian contexts as a result of the Biblical Deluge, for Neoplatonic thought, which influenced early Christian writers, assumed that a perfect Creation would have to have been in the form of a perfect sphere. Such thinking persisted into the eighteenth century.
   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 orogenic belts created and contained. 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, contested hotly 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) drew attention to the metamorphic differences in orogenic belts, proposing three types, modified by W. S. Pitcher (1979);

Hercynotype (back-arc basin type);
- Shallow, low-pressure metamorphism; thin metamorphic zones
- Metamorphism dependent on increase in temperature
- Abundant granite and migmatite
- Few ophiolites, ultramafic rocks virtually absent
- very wide orogen with small and slow uplift
- nappe structures rare
Alpinotype (ocean trench style);
- deep, high pressure, thick metamorphic zones
- metamorphism of many facies, dependent on decrease in pressure
- few granites or migmatites
- abundant ophiolites with ultramafic rocks
- Relatively narrow orogen with large and rapid uplift
- Nappe structures predominant
Cordilleran (arc) type;
- dominated by calc-alkaline igneous rocks,andesites, granite batholiths
- general lack of migmatites, low geothermal gradient
- lack of ophiolite and abyssal sedimentary rocks (black shale, chert, etcetera)
- low-pressure metamorphism, moderate uplift
- lack of nappes

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.

Physiography

The process of orogeny can take tens of millions of years and build mountains from plains or even the ocean floor. Orogeny can occur due to continental collision or volcanic activity. 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).
Orogeny usually produces long linear 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. These island arcs may be added to a continent during an orogenic event.

List of orogenies

North American orogenies

Wopmay orogeny

Along western edge of Canadian shield, 2100-1900 mya.

Hudsonian orogeny or Trans-Hudson orogeny

Extends from Hudson Bay west into Saskatchewan then south through the western Dakotas and Nebraska. Result of the collision of the Superior craton with the Hearne craton and the Wyoming craton during the Proterozoic.
Lasted from 2000-1800 mya.

Penokean orogeny

Wisconsin, Minnesota, and Michigan, U. S. A. and southern Ontario, Canada, 1850-1840 mya.

Big Sky orogeny

Proterozoic collision between the Hearne craton and the Wyoming craton in southwest Montana, 1770 mya.

Ivanpah orogeny

Mojave province, south western USA

Yavapai orogeny

mid to south western USA, circa 1750 mya.

Mazatzal orogeny

mid to south western USA, circa 1600 mya.

Grenville orogeny

Worldwide during the late Proterozoic, 1300-1000 mya. Associated with the assembly of the supercontinent Rodinia. Formed folded mountains in Eastern North America from Newfoundland to North Carolina, 1100-1000 mya.

Caledonian orogeny

the Taconic phase in the NE U.S. and Canada during the Ordovician Period.
the Acadian phase in the Eastern U.S. during Silurian and Devonian Periods.

Appalachian orogeny, usually seen as the same as the Variscan orogeny in Europe.

Appalachian Mountains is a well studied orogenic belt resulting from a late Paleozoic collision between North America and Africa.
Taconic orogeny
Acadian orogeny
Alleghenian orogeny

Ouachita orogeny

Ouachita Mountains of Arkansas and Oklahoma is an orogenic belt that dates from the late Paleozoic Era and is most likely a continuation of the Appalachian orogeny west across the Mississippi embayment - Reelfoot Rift zone.

Antler orogeny

Ancestral Sierra Nevada western United States.
Late Devonian - early Mississippian.

Innuitian orogeny or Ellesmerian orogeny

Innuitian Mountains, Canadian Arctic, extending from Ellesmere Island to Melville Island, Mississippian 345 mya.

Sonoma orogeny

Rocky Mountains, western North America, 270 - 240 million years ago.

Nevadan orogeny

Developed along western North America during the Jurassic Period.

Sevier orogeny

Rocky Mountains, western North America, 140 - 50 million years ago.

Laramide orogeny

Rocky Mountains, western North America, 40-70 Myr ago.

European orogenies

The Caledonian orogeny

Formation of the highlands of western Norway, Britain and Ireland in the Silurian Period.

Uralian orogeny

Formation of the Ural Mountains, Eurasia, during the Permian Period.

The Variscan orogeny (also called the Hercynian orogeny)

Formation of the mountains of western Iberia, SW Ireland, SW England, central France, southern Germany and Czechoslovakia during the Devonian and Carboniferous Periods.

The Alpine orogeny, encompassing:

the Formation of the Alps during the Eocene through Miocene Periods.
the Carpathian orogeny building the Carpathian Mountains of eastern Europe during the Miocene Period.
the Hellenic orogeny in Greece and the Aegean area during Eocene through Miocene Periods.

Ongoing (happening now):

the Mediterranean Ridge.

Asian orogenies

The Aravalli-Delhi Orogen (precambrian)

The Altaid Orogeny (Paleozoic)

The Cimmerian and Cathayasian orogenies

Active through Triassic and Jurassic Periods along south and southeast Asia.

Alpine orogeny, encompassing:

The Himalayan orogeny, forming the Himalaya Mountains, as a result of the ongoing collision of the Indian Plate with the Eurasian Plate.

South American orogenies

Andean orogeny

Andes Mountains, 0-200 Myr ago.

African orogenies

Pan-African orogeny (Neoproterozoic)

Damaran Orogeny

Australian orogenies

Sleaford Orogeny (2440-2420 Ma), Gawler Craton, South Australia

Glenburgh Orogeny (c. 2005 - 1920 Ma), Glenburgh Terrane, Western Australia.

Kimban Orogeny (c. 1845-1700 Ma), Gawler Craton, South Australia

Yapungku Orogeny (c. 1700 Ma), North Yilgarn craton margin, Western Australia

Mangaroon Orogeny (c.1680 - 1620 Ma), Gascoyne Complex, Western Australia.

Kararan Orogeny (1650- Ma), Gawler Craton, South Australia

Barramundi Orogeny (c. 1600 Ma), MacArthur Basin, northern Australia

Isan Orogeny, c. 1600 Ma, Mt Isa Block, Queensland

Olarian Orogeny, Olary Block, South Australia

Capricorn Orogeny, Gascoyne Complex, Western Australia

Musgrave Orogeny (c. 1080 Ma), Musgrave Block, Central Australia.

Edmundian Orogeny (c. 920 - 850 Ma), Gascoyne Complex, Western Australia.

Petermann Orogeny (c. 550-535 Ma late Neoproterozoic to Cambrian), Central Australia

Delamerian Orogeny, South Australia and Victoria, Australia, Ordovician

Lachlan Orogeny, c. 540 and 440 Ma., Victoria and New South Wales

Alice Springs Orogeny in central Australia, Early Carboniferous

Hunter-Bowen Orogeny, (c. 260 - 225 Ma) Permian to Triassic, Queensland and New South Wales

Antarctic orogenies

Napier orogeny (4000 ± 200 Myr ago.)

Rayner orogeny (~ 3500 Myr ago.)

Humboldt orogeny (~ 3000 Myr ago.)

Insel orogeny (2650 ± 150 Myr ago.)

Early Ruker orogeny (2000 - 1700 Myr ago.)

Late Ruker / Nimrod orogeny (1000 ± 150 Myr ago.)

Beardmore orogeny (633 - 620 Myr ago.)

Ross Orogeny (~ 500 Myr ago.)

New Zealand orogenies

Tuhua Orogeny (370 to 330 Myr ago)

Rangitata Orogeny (142 to 99 million years ago)

Kaikoura Orogeny (24 million years ago to present day)Further Information

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