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a) The Magma (Introduction)

name means magma matter in semi-fluid state -result of the merger of silicates and other compounds that make up the rocks, which show properties that do not correspond with the solid state and also with those of a liquid or fluid, according to general principles of physics. The magma
appear in different types of suspension crystals and fragments partially melted rocks and carbonates, sulfides and other components dissolved volatile.
The interaction of different physical conditions determine the characteristics of magma, both in terms of their chemical composition and its viscosity, strength, plasticity and movement.

magmas types
A first classification of different types of magmas refers to its silica content. magmas with more than 60% silica dioxide are called acids, while those with less that amount are called basic .

When magma is reaching out for the weakest points of the earth's crust, magma bodies give rise to volcanoes and formed by cooling magmatic rocks, also called igneous or eruptive, whose degree of crystallization is variable, and among them are granite, basalt or porphyry.
The ascent of magma depends on its physical-chemical conditions (Viscosity, density, content of volatile elements, etc.) Of the particular tectonic region where rocks and have to cross. The

acid magmas are light and viscous, rise with ease and create large reservoirs. The basic magmas
, higher density, less viscous and ascend more difficult than previous ones.

When mixtures of various substances, the magmas do not have a melting point defined, but a melting range. Similarly, no one can speak of crystallization temperature, but crystallization interval.

PHYSICAL PROPERTIES OF MAGMA

The physical properties of magmas vary with temperature, pressure, chemical composition and other parameters such as crystallinity and gallbladder. The two most important properties of magmas are the density and viscosity. Density

Small compositional differences can produce substantial changes in density. The molten basalt, andesite and rhyolite in liquidus temperatures have densities gm/cm3 2.7,2.5 and 2.3, respectively. Density changes associated with cooling are smaller than density changes caused by differentiation from a basaltic liquid with a rhyolite.
a melt density decreases during cooling due to crystallization of the melt separating elements more volatile densos.los have a significant effect on the density, such as water coming down the density of the fluid.

Viscosity
A silica-rich melt, such as rhyolite, is composed of long chains and rings of silica tetrahedra. Consequently, rhyolitic melts have very high viscosity, while the basalt have much lower viscosities. The viscosity also depends strongly on the temperature.
The effect of pressure es todavía desconocido, pero algunos datos experimentales indican un descenso de la viscosidad con el incremento de la presión.

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b) Magmatic Differentiation

Cristalización magmática
      El magma se origina cuando en un lugar de la corteza o del manto superior la temperatura alcanza un punto en el que los minerales con menor punto de fusión empiezan a fundirse (inicio de fusión parcial de las rocas).
      Sin embargo, la temperatura de fusión no depende sólo del tipo de roca, sino también other factors such as the pressure he is or the presence or absence of water.
The increased pressure able to absence of water makes the merger , therefore, with depth, tends to increase the melting temperature of the rocks. By contrast, the presence of water decreases the melting point .

After its formation, the magma rises, it is less dense than the surrounding rocks. During ascent cools and begins to crystallize , Forming minerals with the lowest ever temperature, according to an orderly sequence known as a series of crystallization of Bowen.

The series Bowen refers to two main lines of crystallization. One indicates the order in which they are silicates rich in iron and magnesium (called ferromagnesian). Discontinuous series called because the crystals formed will be replaced by others with different and more complex structure as the temperature drops.
The another series of crystallization is that of plagioclase . called be of continuing trained on because the minerals have the same structure and only changes the relative proportion of sodium and calcium. At the end of crystallization, while sodium plagioclase (albite) and the lenses are formed quartz and orthoclase. Magmatic differentiation


sometimes occurs as the crystallization of a magma when the density difference between minerals and liquid formed and the residual is high and if This viscosity is low, crystals newly formed can be isolated from the rest of the magma, which therefore will be progressively enriched in silica.
to continue the process will produce, from a single magma, a series of igneous rocks of different composition, fractional crystallization . This process is called magmatic differentiation, and may originally acidic rock formation from basic to intermediate magmas. Phases


The magmatic crystallization cooling of magma within the crust results in a series of successive phases of crystallization, lower and lower temperatures.
The first is called ortomagmática phase, which generally occurs from above 700 ° C (depending on the composition of other physical conditions .) It crystallizes most of the magma forming plutonic rocks.

pegmatitic phase takes place more or less between 700 and 550 º C . At these temperatures, the residual melt is very rich in volatiles , so you enter through cracks, which crystallizes causing yacimentos Philonian of pegmatites. The minerals are silicates are rich in silica (quartz, orthoclase, albite), hydroxyl group (micas) and elements such as boron (tourmaline), phosphorus (apatite), fluoride (fluorite), etc.
In the third phase, called neumatolítica , which takes place about the 550 and 375 ° C , crystallizing the residue is composed mainly of volatile , which penetrate the host rocks and veins leading to consist of minerals such as muscovite, quartz, topaz, oxides and metal sulfides, etc. . Similarly, acting on volatile minerals of igneous rocks sticking or transforming them.
The last stage, called hydrothermal , starts below 375 ° C results in streaks and veins of quartz and calcite, a mineral and metal transformation minerals already formed.

magmatism and plate tectonics
The origin of magma is often associated with the global dynamics of the crust and mantle, and that, in general, takes place at the edges of plates. The dorsal
, the magma is basically formed by decompression of the upper mantle materials, shallow, and leads to basic rocks (basalts and gabbros) . In
subduction zones, magma originates at a depth of 150 km from partial melting of oceanic crust and / or the mantle and crust located above. This process results in the formation of rocks mostly intermediate (andesites and granodiorites).
In areas of continental collision in relation to orogenic processes, there is partial melting of the crust, and there are essentially acidic rocks like granite. There are also
specific areas of intraplate magmatism, which is due to the existence of hot spots in the mantle.

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c) Magmas as composition

genres magmas on Earth are due to the existence of convective currents in the mantle and the relative movements of lithospheric plates.

magmatism in the ocean is dominated by the generation of basalt. Small amounts of felsic or silicic magmas formed in the ridges, are linked to long with the basalts by processes of differentiation. On the continents, the magmatism is much more complex and diverse.
to describe this type of magmatism may be considered three main categories within the continental volcanism:

• FLOOD BASALT

Certain volcanic provinces are characterized by the formation of a large number of lava flows, with large volumes of hundreds of cubic miles. The basalts are

toleíca composition suggesting an extensive partial melting in the mantle. Large amounts of melt can be interpreted as the consequence of decompression in the mantle.

• alkaline magmatism

There is a wide and bewildering variety of igneous alkaline silica-deficient, incluyenfo alkali basalts, basanites and nephelinite, can also be grouped carbonalitas and kimberlites. but these rock types do not lead to the same origin.

There is sufficient evidence to believe that parts of the continental lithospheric mantle are very aniguas and in some places have been invaded by volatile components, mainly water and carbon dioxide.

• MAGMATISM SILICEA

The most important category within the continental volcanism, as it involves the development of large volumes of intermediate and silicic magmas, which often predominate over basaltic products. In the plutonic environment rocs form as diorite, tonalite, and granite ganodiorita whereas in volcanic environments range formaanrocas andesite-dacite-rhyolite. There

Two main hypotheses on the origin of siliceous amgmas. First is the idea that, since the continental crust is made up of granitic materials, these magmas are the result of a simple remelting of the crust. Second, siliceous magmas are formed by differentiation of basaltic magmas generated in the mantle.

siliceous magmas have much higher viscosities than basaltic magmas. These viscosities as high have important implications for the mechanisms of segregation and ascent of magma. This implies that the siliceous magmas must rise as masses rather than through narrow cracks.

crystallization along the margins of the chamber is a possible mechanism for differentiation and zonation of siliceous magmas.