Syenite is an uncommon, coarse-grained, intrusive igneous rock. It has the same general composition as granite, but the quartz component is either absent or present in relatively small amounts (less than five percent). The predominant minerals in syenite belong to the feldspar group. The different varieties of syenite are named on the basis of additional minerals in the rock—for example, hornblende syenite and mica syenite. Syenites are occasionally used as building stones.
The term syenite was originally applied to hornblende granite like that obtained from Syene in Egypt, from which the name is derived.
Syenites are usually either peralkaline (in which the molecular proportion of aluminum is less than that of sodium oxide and potassium oxide combined) or peraluminous (in which the molecular proportion of aluminum oxide is greater than that of sodium oxide and potassium oxide combined).
The feldspar component of syenite is predominantly alkaline in character (usually orthoclase). Plagioclase feldspars may be present in small quantities—less than ten percent.
Formation and occurrence
Syenites are formed during alkaline igneous activity, generally formed in thick continental crustal areas, or in Cordilleran subduction zones. A syenite is produced when a granitic or igneous rock undergoes a fairly low degree of partial melting—a condition that is required because potassium is an incompatible element and tends to enter a melt first. Higher degrees of partial melting will liberate more calcium and sodium, producing plagioclase, and hence a granite, adamellite or tonalite.
At very low degrees of partial melting a silica undersaturated melt is produced, forming a nepheline syenite, where orthoclase is replaced by a feldspathoid such as leucite, nepheline or analcime.
Episyenite (or epi-syenite) is a term used in petrology to describe the result of alteration of a SiO2-rich rock to a more SiO2-depleted rock. The term stems from "epi" and syenite.
The process that results in SiO2 depletion can be termed episyenitization. This process is only referring to the macroscopic result of relative SiO2 depletion in a rock. The actual physical process leading to this SiO2 depletion may vary in a given metamorphic environment. Diffusion of chemical components in a stagnant fluid, related to differences in chemical potential or pressure, as well as advection of a SiO2- undersaturated fluid, may lead to the dissolution of quartz from the unaltered rock, thus depleting it of this component.
- Blatt, Harvey, and Robert J. Tracy. 1995. Petrology: Igneous, Sedimentary, and Metamorphic, 2nd ed. New York: W. H. Freeman. ISBN 0716724383
- Pellant, Chris. 2002. Rocks and Minerals. Smithsonian Handbooks. New York: Dorling Kindersley. ISBN 0789491060
- Shaffer, Paul R., Herbert S. Zim, and Raymond Perlman. 2001. Rocks, Gems and Minerals. Revised ed. New York: St. Martin's Press. ISBN 1582381321
New World Encyclopedia writers and editors rewrote and completed the Wikipedia article in accordance with New World Encyclopedia standards. This article abides by terms of the Creative Commons CC-by-sa 3.0 License (CC-by-sa), which may be used and disseminated with proper attribution. Credit is due under the terms of this license that can reference both the New World Encyclopedia contributors and the selfless volunteer contributors of the Wikimedia Foundation. To cite this article click here for a list of acceptable citing formats.The history of earlier contributions by wikipedians is accessible to researchers here:
The history of this article since it was imported to New World Encyclopedia:
Note: Some restrictions may apply to use of individual images which are separately licensed.