intrusion

This article is largely based on an article in the out-of-copyright 11th edition of the Encyclopædia Britannica, which was produced in 1911. It should be brought up to date to reflect subsequent history or scholarship (including the references, if any). When you have completed the review, replace this notice with a simple note on this article's talk page. Thanks! (January 2011)

Devils Tower National Monument, an igneous intrusion exposed when the surrounding softer rock eroded away.

An intrusion is liquid rock that forms under Earth's surface. Magma from under the surface is slowly pushed up from deep within the earth into any cracks or spaces it can find, sometimes pushing existing country rock out of the way, a process that can take millions of years. As the rock slowly cools into a solid, the different parts of the magma crystallize into minerals. Many mountain ranges, such as the Sierra Nevada in California, are formed mostly by intrusive rock, large granite (or related rock) formations.

Intrusions are one of the two ways igneous rock can form; the other is extrusive, that is, a volcano eruption or similar event. Technically speaking, an intrusion is any formation of intrusive igneous rock; rock formed from magma that cools and solidifies within the crust of a planet. In contrast, an extrusion consists of extrusive rock; rock formed above the surface of the crust.

Intrusions vary widely, from mountain range sized batholiths to thin vein-like fracture fillings of aplite or pegmatite. When exposed by erosion, these cores called batholiths may occupy huge areas of Earth's surface. Large bodies of magma that solidify underground before they reach the surface of the crust are called plutons.

Coarse grained intrusive igneous rocks that form at depth within the earth are called abyssal while those that form near the surface are called hypabyssal. Intrusive structures are often classified according to whether or not they are parallel to the bedding planes or foliation of the country rock: if the intrusion is parallel the body is concordant, otherwise it is discordant.

A well-known example of an intrusion is Devil's Tower.

Structural types

A dike intrudes into the country rock, Baranof Island, Alaska, USA.

Intrusions can be classified according to the shape and size of the intrusive body and its relation to the other formations into which it intrudes:

Batholith: a large irregular discordant intrusion

Dike: a relatively narrow tabular discordant body, often nearly vertical

Laccolith: concordant body with roughly flat base and convex top, usually with a feeder pipe below

Lopolith: concordant body with roughly flat top and a shallow convex base, may have a feeder dike or pipe below

Phacolith: a concordant lens-shaped pluton that typically occupies the crest of an anticline or trough of a syncline

Volcanic pipe or volcanic neck: tubular roughly vertical body that may have been a feeder vent for a volcano

Sill: a relatively thin tabular concordant body intruded along bedding planes

Stock: a smaller irregular discordant intrusion

Characteristics

An intrusion (pink Notch Peak monzonite) inter-fingers (partly as a dike) with highly-metamorphosed black-and-white-striped host rock (Cambrian carbonate rocks). Near Notch Peak, House Range, Utah.

Deep-seated intrusions are recognized from the way they have burst through the overlaying strata. Ramifying veins result from filled cracks, and the high temperature involved in this process is evident from the altered adjacent country rock. Since heat dissipates slowly and since the rock is under pressure, crystals form and no vitreous rapidly chilled matter is present. As the intrusions have had time to rest before crystallizing, they are not fluidal. Their contained gases have not been able to escape through the thick layer of strata, beneath which they were injected. Such gases form cavities, which can often be observed in these minerals. Such gases have also resulted in many important modifications in the crystallization of the rock. Because their crystals are of approximately equal size these rocks are said to be granular.

There is typically no distinction between a first generation of large well-shaped crystals and a fine-grained ground-mass. The minerals of each have formed in a definite order, and each has had a period of crystallization that may be very distinct or may have coincided with or overlapped the period of formation of some of the other ingredients. Earlier crystals originated at a time when most of the rock was still liquid and are more or less perfect. Later crystals are less regular in shape because they were compelled to occupy the spaces left between the already-formed crystals. The former case is said to be idiomorphic (or automorphic); the latter is xenomorphic. There are also many other characteristics that serve to distinguish the members of these two groups. For example, orthoclase is typically feldspar from granite, while its modifications occur in lavas of similar composition. The same distinction holds for nepheline varieties. Leucite is common in lavas but very rare in plutonic rocks. Muscovite is confined to intrusions. These differences show the influence of the physical conditions under which consolidation takes place.

Some intrusive rocks solidified in fissures as dikes and intrusive sills at a shallow depth beneath the surface and are called hypabyssal. Those formed at greater depths are called plutonic or abyssal. As might be expected, they show structures intermediate between those of extrusive and plutonic rocks. They are very commonly porphyritic, vitreous, and sometimes even vesicular. In fact, many of them are petrologically indistinguishable from lavas of similar composition.^[1]

See also

• Pluton
• Volcanic rock

References

1. ^  This article incorporates text from a publication now in the public domain: Chisholm, Hugh, ed (1911). "Petrology". Encyclopædia Britannica (11th ed.). Cambridge University Press. 

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