Class Notes (1,100,000)
CA (630,000)
McGill (30,000)
EPSC (200)
EPSC 201 (100)
Lecture 14

EPSC 201 Lecture Notes - Lecture 14: Biotite, Devitrification, Plagio


Department
Earth & Planetary Sciences
Course Code
EPSC 201
Professor
Anthony Williams- Jones
Lecture
14

This preview shows pages 1-2. to view the full 6 pages of the document.
EPSC201 - Lecture 14 Notes
If an earthquake is along a transform fault, they
don’t generate as much surface waves. Surface
waves are responsible for damage. If its along
a transform fault, the direction it should slide is
already defined and set up to move.
Here are some types of intrusive rock
Laccolith – a huge underground body of mag-
ma, that can cool, and pushes up the sedimen-
tary layers above it
Batholith – main magma chamber that feeds all
these other terms. If the sedimentary layers
wear down enough, it will become exposed.
They look like rounded out-
crops formed from igneous rocks. These can be very large, up to 50 km wide. So
these are large bodies of magma.
Dike – vertical wall of hard rock, it would have fed a fissure eruption of magma go-
ing upwards, can be thin but continue onwards for kilometers. They feed volca-
noes by flowing upwards.
Sill – horizontal intrusions of magma that
go in-between layers of sedimentary rock, fed by dikes, can be
very thick, or very thin. Hundreds of meters to cm thick.
Diabase – intrusive basaltic rock, does not make it to the sur-
face – form of gabbro
Gabbro – intrusive igneous rock chemically equivalent to basalt
Basalt – extrusive, the magma makes it out to the surface
Why do we get magma formation and volcanoes? Why do we
get hot spots, such as Hawaii and Iceland?
With spreading activity, you get basalt. With subduction, you
get andosite and rhyolite.
At spreading centers, we have decompression melting. As the
plates spread, mantle moves upwards, and releases pressure.
This causes the mantle to melt.

Only pages 1-2 are available for preview. Some parts have been intentionally blurred.

Rocks are great insulators. As the mantle moves upwards,
the surrounding rocks stay hot (the temperature they were
when deep). So the mantle rises up, and is under less tem-
perature, but is at the same hot temperature. This causes the
mantle to melt into magma, and is called decompression
melting.
Shown here is a geotherm. From this, we see that as pres-
sure increases going deeper into the earth, higher tempera-
tures are required to make the rock liquid.
At the liquids line, everything right of the line is liquid, which
shows that at higher temperatures, the rock turns to liquid.
Anything on the solidus line that is moved upwards due
to mantle upwelling (decompression melting) will then
turn to liquid. This graph explains why decompression
melting works. However, the mantle must move enough
to reach the liquidus line. If it only moves a little bit, and
doesn’t reach the next line, it won’t melt completely. Of-
ten, the mantle will be in a state of partial liquids and
partial solidus.
Subducting slabs come from the surface, which is at a
much colder temperature then the mantle. Nonetheless,
we still observe magma formation due to melting of the
subducting slab. The friction of the subducting slab also
causes a small amount of heating, but is not the source
of melting.
The source of melting for the subducting plate is water.
If the subducting plate has water content, the melting
point of the solidus is much lower. The above geotherm
assumes the conditions are anhydrous. However, if
there is water present then things melt much easier.
Subducting plates often come from ocean, which causes
them to have high water content.
Here the subducting plate is under the ocean. This
drags down seawater, which hydrates them. Note the
different geotherms for hydrated and dehydrated plate
melting. The hydrated form melts much easier.
You're Reading a Preview

Unlock to view full version