dif magm tica mezcla de magmas 2015

8/17/2019 Dif Magm Tica Mezcla de Magmas 2015

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Diferenciación magmática


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Cristalización en equilibrio y

fraccionada

Composición inicial vs. Composiciónfinal

Li

L f

Si

S f


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Fraccionamiento gravitacional

Fraccionamiento de sólidos, líquido yburbujas


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Ley de Stokes

V = velocidad de decantación (cm/sec)g = aceleración de gravedad (980 cm/sec2)r = radio de una partícula sólida esférica (cm)ρs = densidad de la partícula sólida esférica

(g/cm3

)ρl = densidad del líquido (g/cm3)η = viscosidad del líquido (Pa s)

V 2gr ( )9

2

= − ρ ρ η s l


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Líquido basáltico

• Olivino (ρs

= 3.3 g/cm3, r = 0.1 cm)

• Líquido Basaltico (ρl = 2.65 g/cm3, η =1000 poise)

• V = 2·980·0.12

(3.3-2.65)/9·1000 =0.0013 cm/seg; aprox. 5 cm/hora


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Líquido riolítico η = 107 poise y ρl = 2.3 g/cm3

• cristal de hornblenda (ρs = 3.2 g/cm3, r =0.1 cm)V = 2 x 10-7 cm/sec, o 6 cm/año

• feldspatos (ρl = 2.7 g/cm3), r = 0.1 cm)V = 2 cm/año = 200 m en los 104 añost que demora en solidificarse un stock

Un cristal de 0.5 cm de radio decanta a0.65 metros/año, o 6.5 km en los 104 años de enfriamiento


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Fraccionamiento Gravitacional de

Cristales


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Adcumulada (0-7 %), mesocumulada (7-15%), ortocumulada (15-25%)


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Cross section lookingdown dip.

Figure 12-11. After After

Hoover (1978) Carnegie Inst.

Wash., Yearb., 77, 732-739.


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Fractionation density vs dif ferentiation index (DI) for plagioclase, where DI = An/(An + Ab),

and for olivine, orthopyroxene, clinopyroxene and pigeonite, where DI = Mg/(Mg + Fe2+).

SCOATES J S J. Petrology

2000;41:627-649Oxford University Press


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LangmuirModel

Thermal gradientat wall and cap→ variation in %crystallized

Compositionalconvection → evolved magmasfrom boundarylayer to cap (ormix into interior)

Figure 11-12 Formation of boundary

layers along the walls and top of a

magma chamber. From Winter

(2001) An Introduction to Igneous

and Metamorphic Petrology.

Prentice Hall

Fraccionamiento convectivo


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Cristales y antecristales


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COEFICIENTE DE EXPANSIÓNTERMAL: Cambio proporcional devolumen por cada °C, a P = cte.3.0 x 10-5 °C-1

http://www.google.cl/url?sa=i&rct=j&q=magma+density+and+temperature&source=images&cd=&cad=rja&docid=XedFlXzuInZH6M&tbnid=l0Ldt95iXO7JeM:&ved=0CAUQjRw&url=http://www.eos.ubc.ca/resources/webres/concepts/igneous/magma/magcont.html&ei=-wNbUYaKNoy68wTqlYCQCA&psig=AFQjCNEXruMcqqjSRhv3KKUdKcap2Lykow&ust=1365005663646100


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Simulación numérica tiempo-

dependiente


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No sepuedemostrarla imagen en estemomento.

( ) r 2

r r r

r r T T z,k =t

T Cp ρ ∇

∂

∂

Heat transfer into the country rocks


( ) ( ) g ρ p' u+u µ=uu+t

u ρ

−∇−∇∇⋅∇

∇⋅

∂

∂

Magma fluid dynamics

where g is the gravity acceleration vector; u is the magma

velocity; p is the pressure; and µ is the dynamic viscosity

ρr r is the density; Cpr is the heat capacity; T r is the

temperature; and k r is the thermal conductivity of the

rock

Numerical simulation


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Exsolución de fases y

composición de líquidos y

magmas


∇⋅∂∂−∇⋅

∂∂ T u+

t

T Q=u+

t j j j j

j φ

φ

the volume fraction of the exsolved phases ( phi j )are explicit functions of temperature onlywhere u j is the exsolved phase movement velocity, and Qj isthe phase exsolution rate


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Gutiérrez & Parada 2010. Journal of Petrology, 51, 731-762

Composiciónde magma yflujomagmático


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Porcentaje de fases a los 10 ky


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Temperaturas con el tiempo


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A los 10 mil años


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Mezcla de magmas


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Enclaves magmáticos vs. xenolitos


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Enlaves magmáticos


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Rol de la reología


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Role of rheology I


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Role of rheology I


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Role of rheology II


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Role of rheology II


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Role of rheology III


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Role of rheology III


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Rol de reología


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Role of rheology IV

Pluton as crystal


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Pluton as crystalmush


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Calentamiento

Automezcla convectiva

Co-existencia de ≠ Plg

dif magm tica mezcla de magmas 2015

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