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What happens to our PROTOLITH when acted on by AGENTS OF CHANGE??. Agents of Change  T, P, fluids, stress, strain Metamorphic Reactions!!!! Solid-solid phase transformation Solid-solid net-transfer Dehydration Hydration Decarbonation Carbonation. Solid-solid phase transformation.

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what happens to our protolith when acted on by agents of change
What happens to our PROTOLITH when acted on by AGENTS OF CHANGE??
  • Agents of Change  T, P, fluids, stress, strain
  • Metamorphic Reactions!!!!
    • Solid-solid phase transformation
    • Solid-solid net-transfer
    • Dehydration
    • Hydration
    • Decarbonation
    • Carbonation
solid solid phase transformation
Solid-solid phase transformation
  • Polymorphic reaction  a mineral reacts to form a polymorph of that mineral
  • No transfer of matter, only a rearrangment of the mineral structure
  • Example:
    • Andalusite  Sillimanite

Al2SiO5

Al2SiO5

solid solid net transfer
Solid-solid net-transfer
  • Involve solids only
  • Differ from polymorphic transformations: involve solids of differing composition, and thus material must diffuse from one site to another for the reaction to proceed
  • Examples:
  • NaAlSi2O6 + SiO2 = NaAlSi3O8

Jd Qtz Ab

  • MgSiO3 + CaAl2Si2O8 = CaMgSi2O6 + Al2SiO5

En An Di And

solid solid net transfer ii

Solid-Solid Net-Transfer II

If minerals contain volatiles, the volatiles must be conserved in the reaction so that no fluid phase is generated or consumed

For example, the reaction:

Mg3Si4O10(OH)2 + 4 MgSiO3 = Mg7Si8O22(OH)2

Talc Enstatite Anthophyllite

involves hydrous phases, but conserves H2O

It may therefore be treated as a solid-solid net-transfer reaction

hydration dehydration reactions
Hydration/ Dehydration Reactions
  • Metamorphic reactions involving the expulsion or incorporation of water (H2O)
  • Example:
    • Al2Si4O10(OH)2 <=> Al2SiO5 + 3SiO2 + H2O

Pyrophyllite And/Ky Quartz water

carbonation decarbonation reactions
Carbonation / Decarbonation Reactions
  • Reactions that involve the evolution or consumption of CO2
  • CaCO3 + SiO2 = CaSiO3 + CO2

calcite quartz wollastonite

Reactions involving gas phases are also known as volatilization or devoltilization reactions

These reactions can also occur with other gases such as CH4 (methane), H2, H2S, O2, NH4+ (ammonia) – but they are not as common

systems
Systems
  • Rock made of different minerals
  • Metamorphic agents of change beat on it  metamorphic reactions occur
  • A closed system does not gain or lose material of any kind
  • An open system can lose stuff – liquids, gases especially

Outside

world

Hunk o’ rock

thermodynamics primer
Thermodynamics Primer
  • Thermodynamics describes IF a reaction CAN occur at some condition (T, P, composition typically)
  • Second Law of thermodynamics:
  • DG=DH – TDS
    • Where G, Gibb’s free energy determines IF the REACTION will go forward (-DG=spontaneous)
    • H is enthalpy – has to do with heat…
    • S is entropy – has to do with bonds and order…
thermodynamics vs kinetics
Thermodynamics vs. Kinetics
  • Thermodynamics – comparing the potential ENERGY of things  what is more stable? Will a reaction occur at some T,P, soln, melt composition go or Not?
  • Kinetics  IF thermodynamics says YES, the reaction should occur (always toward lower energy!) kinetics determines how fast
  • Minerals out of equilibrium pass the thermodynamic test but the kinetics of their reaction is very slow…
phase diagrams
Phase diagrams
  • Tool for ‘seeing’ phase transitions
  • H2Oice H2Oliquid
  • Reaction (line) governed

by DG=DH – TDS

  • Phase Rule:
    • P+F=C+2
    • Phases coexisting + degrees of freedom = number of components + 2
    • Degree of freedom  2= either axis can change and the phase stays the same  where??
phase diagrams1
Phase diagrams
  • Let’s think about what happens to water as conditions change…
  • P+F=C+2
  • Point A?
  • Point B?
  • Point C?

A

B

C

mineral assemblages in metamorphic rocks
Mineral Assemblages in Metamorphic Rocks
  • Equilibrium Mineral Assemblages
  • At equilibrium, the mineralogy (and the composition of each mineral) is determined by T, P, and X
  • Relict minerals or later alteration products are thereby excluded from consideration unless specifically stated
the phase rule in metamorphic systems
The Phase Rule in Metamorphic Systems
  • Phase rule, as applied to systems at equilibrium:

F = C - P + 2 the phase rule

P is the number of phases in the system

C is the number of components: the minimum number of chemical constituents required to specify every phase in the system

F is the number of degrees of freedom: the number of independently variable intensive parameters of state (such as temperature, pressure, the composition of each phase, etc.)

the phase rule in metamorphic systems1
The Phase Rule in Metamorphic Systems

C = 1 (Al2SiO5)

  • F = 1 common
  • F = 2 rare
  • F = 3 only at the specific P-T conditions of the invariant point

(~ 0.37 GPa and 500oC)

Consider the following three scenarios:

Figure 21-9. The P-T phase diagram for the system Al2SiO5 calculated using the program TWQ (Berman, 1988, 1990, 1991). Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.

metamorphic facies
Metamorphic facies
  • P-T conditions, presence of fluids induces different metamorphic mineral assemblages (governed by thermodynamics/ kinetics)
  • These assemblages are lumped into metamorphic facies (or grades)
aluminosilicate minerals
Aluminosilicate Minerals
  • SILLIMANITE: Orthorhombic: Octahedral Al chains (6-fold) are crosslinked by both Si and Al tetrahedra (4-fold).
  • ANDALUSITE: Orthorhombic: 5-coordinated Al; Same octahedral (6-fold) chains.
  • KYANITE: Triclinic: All the Al is octahedrally coordinated (6- and 6-fold).

Andalusite

Kyanite

Sillimanite

  • Clearly, changes in structure are in response to changing P and T. Result is changes in Al coordination.
  • Phase transformations require rebonding of Al. Reconstructive polymorphism requires more energy than do displacive transformations. Metastability of these 3 are therefore important (Kinetic factors limit equilibrium attainment).
  • All 3 are VERY important metamorphic index minerals.
aluminosilicate minerals1
Aluminosilicate Minerals
  • 3 polymorphs of Al2SiO5 are important metamorphic minerals

Andalusite

Kyanite

Sillimanite

topaz
Topaz
  • Aluminosilicate mineral as well, one oxygen substituted with OH, F
  • Al2SiO4(F,OH)2
  • Where do you think Topaz forms??
serpentine minerals
Serpentine Minerals
  • Mg3Si2O5(OH)4 minerals (principally as antigorite, lizardite, chrysotile polymorphs)
  • Forms from hydration reaction of magnesium silicates
    • Mg2SiO4 + 3 H2O  Mg3Si2O5(OH)4+ Mg(OH)2

forsterite serpentine brucite

  • Asbestosform variety is chrysotile (accounts for 95% of world’s asbestos production  MUCH LESS DANGEROUS than crocidolite)
slide21

Phyllosilicates

T O - T O - T O

Yellow = (OH)

vdw

Serpentine: Mg3 [Si2O5] (OH)4

T-layers and triocathedral (Mg2+) layers

(OH) at center of T-rings and fill base of VI layer 

vdw

weak van der Waals bonds between T-O groups

slide22

Octahedra are a bit larger than tetrahedral match, so they cause bending of the T-O layers (after Klein and Hurlbut, 1999).

Serpentine

Antigorite maintains a sheet-like form by alternating segments of opposite curvature

Chrysotile does not do this and tends to roll into tubes

slide23

Serpentine

Veblen and Busek, 1979, Science 206, 1398-1400.

S = serpentine T = talc

Nagby and Faust (1956) Am. Mineralogist 41, 817-836.

The rolled tubes in chrysotile resolves the apparent paradox of asbestosform sheet silicates

chlorite
Chlorite
  • Another phyllosilicate, a group of difficult to distinguish minerals
  • Typically green, and the dominant and characteristic mineral of greenschist facies rocks
  • Forms from the alteration of Mg-Fe silicates (pyroxenes, amphiboles, biotite, garnets)
prehnite pumpellyite
Prehnite-Pumpellyite
  • Minerals related to chlorite, form at slightly lower P-T conditions
  • Prehnite is also green, pumpellyite
micas
Micas
  • Biotite and Muscovite are also important metamorphic minerals (muscovite often the principle component of schists)
  • Phlogopite – similar to biotite, but has little iron, forms from Mg-rich carbonate deposits and a common mineral in kimberlites (diamond-bearing material)
  • Sericite – white mica (similar to muscovite) – common product of plagioclase feldspar alteration at low grades
zeolites
Zeolites
  • Diverse group of minerals forming at lower metamorphic grades
  • Framework silicas, but characteristically containing large voids and highly variable amounts of H2O
    • Name is from the greek – meaning to boil stone as the water can de driven off with heat
    • Voids can acts as molecular sieves and traps for many molecules
    • Diversity of minerals in this group makes a for a wide variety of sieve and trapping properties selective for different molecules
epidote group
Epidote Group
  • Sorosilicates (paired silicate tetrahedra)
  • Include the mineral Epidote Ca2FeAl2Si3O12(OH), Zoisite (Ca2Al3Si3O12(OH) and clinozoisite (polymorph)
garnets

Garnet: A2+3 B3+2 [SiO4]3

  • “Pyralspites” - B = Al
    • Pyrope: Mg3 Al2 [SiO4]3
    • Almandine: Fe3 Al2 [SiO4]3
    • Spessartine: Mn3 Al2 [SiO4]3
  • “Ugrandites” - A = Ca
    • Uvarovite: Ca3 Cr2 [SiO4]3
    • Grossularite: Ca3 Al2 [SiO4]3
    • Andradite: Ca3 Fe2 [SiO4]3
  • Occurrence:
    • Mostly metamorphic
    • Some high-Al igneous
    • Also in some mantle peridotites

Garnets

Garnet (001) view blue = Si purple = A turquoise = B

staurolite
Staurolite
  • Aluminosilicate - Fe2Al9Si4O22(OH)2
  • Similar structure to kyanite with tetrahedrally coordinated Fe2+ easily replaced by Zn2+ and Mg2+
  • Medium-grade metamorphic mineral, typically forms around 400-500 C
    • chloritoid + quartz = staurolite + garnet
    • chloritoid + chlorite + muscovite = staurolite + biotite + quartz + water
  • Degrades to almandine (garnet at higher T)
    • staurolite + muscovite + quartz = almandine + aluminosilicate + biotite + water
metamorphic facies1
Metamorphic Facies
  • Where do we find these regimes of P-T ‘off’ of the typical continental isotherms??
  • How is the environment that forms a blueschist facies rock different from one forming a hornfels?
metamorphic facies2

Metamorphic Facies

Table 25-1. The definitive mineral assemblages that characterize each facies (for mafic rocks).

facies series

Facies Series

Miyashiro (1961) initially proposed five facies series, most of them named for a specific representative “type locality” The series were:

1. Contact Facies Series (very low-P)

2. Buchan or Abukuma Facies Series (low-P regional)

3. Barrovian Facies Series (medium-P regional)

4. Sanbagawa Facies Series (high-P, moderate-T)

5. Franciscan Facies Series (high-P, low T)

slide35

Fig. 25-3.Temperature-pressure diagram showing the three major types of metamorphic facies series proposed by Miyashiro (1973, 1994). Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.

isograds
Isograds
  • Lines (on a map) or Surfaces (in the 3D world) marking the appearance or disappearance of the Index minerals in rocks of appropriate compositione.g. the ‘garnet-in isograd’; the ‘staurolite-out isograd’Complicated by the fact that most of these minerals are solid solutions
slide37
Isograds for a single shale unit in southern Vermont
  • Which side reflects a higher grade, or higher P/T environment?
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