Geosyncline

Geosyncline is a geological concept which was developed in the late 19th and early 20th centuries before the concept of plate tectonics was developed. A geosyncline was described as a subsiding linear trough that was caused by the accumulation of sedimentary rock strata deposited in a basin and subsequently compressed, deformed, and uplifted into a mountain range, with attendant volcanism and plutonism. The filling of a geosyncline with sediment is accompanied in the late stages of deposition by folding, crumpling, and faulting of the deposits. Intrusion of crystalline igneous rock and regional uplift along the axis of the trough generally complete the history of a particular geosyncline. It is then transformed into a belt of folded mountains. Thick volcanic sequences, together with greywackes (sandstones rich in rock fragments with a muddy matrix), cherts, and various sediments reflecting deepwater deposition or processes, were considered eugeosynclinal deposits of the outer deepwater segment of geosynclines.

Overview

The geosyncline hypothesis is an obsolete concept[1] involving vertical crustal movement that has been replaced by plate tectonics to explain crustal movement and geologic features.

Geosynclines were divided into miogeosynclines and eugeosynclines, depending on the types of discernible rock strata of the mountain system.

A miogeosyncline develops along a passive margin of a continent and is composed of sediments with limestones, sandstones and shales. The occurrences of limestones and well-sorted quartz sandstones indicate a shallow-water formation.

A eugeosyncline consists of rocks from deep marine environments. Eugeosynclinal rocks include thick sequences of greywackes, cherts, slates, tuffs and submarine lavas. The eugeosynclinal deposits are typically more deformed, metamorphosed, and intruded by small to large igneous plutons. Eugeosynclines often contain flysch typical of a continental-continental convergent boundary.

An orthogeosyncline is a linear geosynclinal belt lying between continental and oceanic terranes, and having internal volcanic belts (eugeosynclinal) and external nonvolcanic belts (miogeosynclinal). Also known as geosynclinal couple or primary geosyncline. A miogeosyncline is the nonvolcanic portion of an orthogeosyncline, located adjacent a craton. A zeugogeosyncline is a geosyncline in a craton or stable area within which is also an uplifted area, receiving clastic sediments, also known as yoked basin. A parageosyncline is an epeirogenic geosynclinal basin located within a craton area. An exogeosyncline is a parageosyncline that lies along the cratonal border and obtains its clastic sediments from erosion of the adjacent orthogeosynclinal belt outside the craton. Also known as delta geosyncline; foredeep; or transverse basin.

Several types of "mobile" geosynclinal zones have also been recognized and named. Among the more common of these are the taphrogeosyncline, a depressed block of the Earth's crust that is bounded by one or more high-angle faults and that serves as a site of sediment accumulation; and the paraliageosyncline, a deep geosyncline that passes into coastal plains along continental margins. It is a naturally occurring phenomenon.

History of the concept

The geosyncline concept was first developed by the American geologists James Hall and James Dwight Dana in the mid-19th century during the classic studies of the Appalachian Mountains.[2] Dana was first to use the term geosynclinal in reference to a gradually deepening and filling basin resulting from his concept of crustal contraction due to a cooling and contracting Earth. The geosynclinal hypothesis was further developed in the late 19th century and early 20th century and at that time was widely accepted as an explanation for the origin of most mountain ranges until its replacement by the subduction zone and continental collision orogenies of plate tectonics in the 1960s. Although the usage varied over the following 100 years, a geosyncline is still basically a large linear deepening basin along a continental margin which becomes deformed and then uplifted in parts as a mountainous region.

See also

References

  1. ↑ Selley, Richard C., Applied Sedimentology, Academic Press, 2nd edition, 2000, p. 486 ISBN 978-0-12-636375-3
  2. ↑ Adolph Knopf, The Geosynclinal Theory, Bulletin of the Geological Society of America 59:649-670, July 1948

Further reading

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