Class Notes (1,100,000)
CA (630,000)
McGill (30,000)
EPSC (200)
EPSC 201 (100)
Lecture 15

EPSC 201 Lecture Notes - Lecture 15: Pyrite, Goethite, Net.

Earth & Planetary Sciences
Course Code
EPSC 201
Anthony Williams- Jones

This preview shows pages 1-2. to view the full 6 pages of the document.
EPSC201 - Lecture 15 Notes
Partial melting – minerals that melt at low temperatures melt into a liquid before minerals with high melt-
ing points. If the mantle is in the range where only some melting occurs, partial melting occurs. The
minerals with lower MPs melt and leave the mantle, forming a magma. The mineral that is last to melt
is magnesium rich olivine. It dominates the mantle, and melts last. Olivine either has iron or magne-
sium. The iron olivine melts at a lower temperature. In general, minerals with high silica content melt
lower (feldspar and quartz). The early magma is enriched in potassium, sodium, and silica, because
these are found in minerals with low MPs. The left over residue that doesn’t melt is called mafic
residue and contains lots of magne-
sium olivine.
Temperature is on the y axis here.
This chart shows which minerals
melt the easiest. What we see is
that as the silicates get more compli-
cated, the temperature of crystalliza-
tion increases (from tetrahedrons to
silicate sheets).
At the bottom, the minerals melt eas-
ily, and have a low MP. At the top of
the chart, the minerals have a high
MP, and crystallize quickly.
Calcium rich plagioclase crystallizes
at a higher temperature then plagioclase with sodi-
um. This mineral crystallizes over quite a interval,
which is termed a continuous series. This chart
can explain most of the igneous rocks in the world.
In the scenario on the left, crystallization is starting to
occur. Convection is occurring in the magma cham-
ber. According to the Bowen series, the olivine will
get converted to the pyroxene, which will eventually
continue to be amphibole…etc. Gradually, the min-
erals change into different minerals. Over time, the
orange (say olivine) will be converted to the blue (say
pyroxene). At the beginning of crystallization, there is
only olivine being crystallized, but as time pro-
gressed, there is a mixture being crystallized. However, as time progresses, the temperature cools.
So by the time olivine is converted to another mineral, it may all be cooled into rock.
As the magma cools, it either crystallizes, or forms a new mineral that has a lower crystallization point.
That’s why on the Bowen Series, we see the arrows pointing to the bottom three minerals.
Low degree of partial melting will make a rhyolite or granite.
High degree of partial melting will make a basalt or gabbro.

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

Medium amount will make an andeosite.
Prof did a horrible job explaining frac-
tional and equilibrium crystallization.
Wikipedia answers….
The process of fractional crystallization
is responsible for the bulk of differentia-
tion that is occurs in igneous rocks.
As ascending melts cool and react with
country rock, those minerals in the melt
that have the highest melting points or
the lowest solubilities (like olivine and py-
roxene) crystallize out first, leaving min-
erals with the lowest melting points be-
hind in the melt to freeze out last.
Gravitative differentiation is the commonest form of fractionation, and results from the phenomenon
that most solid minerals are denser than their parent melts. As denser crystals settle to the bottom of
the magma body, they become segregated from the residual melt. Rocks that are formed by settling
crystals are termed cumulates, and the rocks are often zoned, with the densest, first-formed crystals
accumulated at the base of the magma chamber. Cumulates formed by the lighter crystals occasionally
float to the top, with the lightest at the very top. This process produces layering in igneous rocks.
Key point – large variety of magmas can be pro-
duced from fractional crystallization and partial melt-
Cold environments are dominated by physical weath-
ering, because chemical reactions require heat to
proceed. Chemical weathering is more dominnt in
hot, wet countries. In cold, dry environments, the
physical weathering is dominant.
Sahara desert – dominated by wind, and physical
weathering. Wind and sand act as a sandpaper, and
cause physical weathering.
In cold environments, freeze thaw weathering is a
dominant force. The expansion of water into ice
causes cracks to expand.
Rocks with round edges have been chemically
weathered. Physical weathering give sharp sur-
faces, with breaks and cracks. Outcrops subjected
to chemical weathering will be smooth.
You're Reading a Preview

Unlock to view full version