1. Sheet Silicates
Micas
Chlorite

2. serpentine Mg3Si2O5(OH)4 A B C D

3. The term serpentine refers to three polymorphs (lizardite, antigorite, crysotile) that may occur together and cannot be easily distinguished in thin section.  Serpentine primarily forms by hydrous alteration of olivine, and in some cases pyroxene, and many crustal peridotites are extensively altered to serpentine.  It is typically colourless to pale yellow or pale green in plane light, and is commonly intergrown with opaque magnetite (A).  The very low maximum interference colours of first order white to yellow are evident in B.  In C, the original outlines and internal fracture pattern of olivine grains are highlighted by opaque magnetite.  (Coarse subhedral opaque minerals are primary Cr-spinels grains.)  In D, more highly birefringent calcite and tremolite accompany the serpentine. Serpentine can be confused with pale-coloured varieties of chlorite (Mg-rich), but in serpentine the slow ray is parallel to the fiber length whereas chlorites with Mg/(Mg+Fe) < 0.50 are length fast.  A and B are from the Hunting Hill, Maryland serpentinite and C and D are from a serpentinized peridotite cumulate from the Abitibi Belt, Ontario.  A and B are 2.2 mm across and C and D are 5.5 mm across.  A and C ppl, B and D x-nicols. 

4. Pleochroism: Orange, brown or dark green(A)
trioctahedral
TOT layer + interlayer cation
K (Mg,Fe)3(AlSi3O10)(OH)2
Monoclinic
Space group: C2/m
Pleochroism: Orange, brown or dark green(A)
Moderate relief
Perfect micaceous cleavage
May be dark pleochroic halos
around inclusions of zircon or other mildly
radioactive minerals (B)

5. Perfect cleavage
Dark halos
Dark colour
Strong pleochroism
High refractive indices

6. Strong pleochroism:
From dark brown to light brown
mottled texture

7. dioctahedral
TOT layer + interlayer cation
KAl2(AlSi3O10)(OH)2
Space group: C2/c
Plane-Polarized Light
Low relief
Clear
Perfect micaceous cleavage
(closely spaced cleavage in one (!) direction
Crossed Polarizers
Bright second-and third-order interference colors
Mottled texture

8. Igneous muscovite is generally
colorless with good cleavage.
Distinguishing features:
Lighter than biotite
Higher 2Vx than other micas
Higher birefringence
than clays and chlorite

9. High birefringence
(upper second order)
Mottled texture

10. Muscovite foliation
Sericite: Not really a
Separate species, but
muscovite with low
birefringence.
Probably K+ replaced
by H3O+; i.e. it is
hydromuscovite

11. talc Mg3Si4O10(OH)2 A B C D

12. Talc is colourless in plane polarized light, and its high birefringence causes its relief to change with rotation of the stage (compare A and B which are rotated 90 degrees relative to one another), a feature that can be mistaken for faint pleochroism.  Maximum interference colours are in the third order (C).  Extinction is parallel to cleavage traces and, like the micas, the grains have a mottled or “crinkly” appearance at and near extinction (D).  Talc and muscovite appear very similar in thin section and usually cannot be reliably distinguished based on optical characteristics alone.  Paragenesis, or mineral assemblage, can be a useful guide.  Although muscovite occurs in a wide variety of igneous and metamorphic rocks, talc is rather restricted in occurrence, typically to high magnesium rocks (mafic or ultramafic) in which is it associated with tremolite, dolomite, serpentine, magnesite and other Mg-rich minerals.  Sample is from a talc-tremolite schist from St. Lawrence County, New York.  All views are 2.2 mm across. A and B ppl, C and D x-nicols.

13. prehnite Ca2Al(AlSi3O10)(OH)2B C D D

14. Prehnite occurs in amygdules and veins in low-grade meta-basic rocks (e.g., basalts) but is more common as a constituent of low-grade meta-greywackes and meta-basic rocks where it is typically too fine-grained for identification by optical techniques.  It is colourless in plane light (A) and has moderately high positive relief relative to quartz and sodic plagioclase, with which it is commonly associated.  In image A prehnite dominates the amygdule and stands out relative to minor interstitial quartz and a quartz core.  In amygdules and veins it commonly forms radiating sheaves, apparent in crossed nicol views B and D.  Maximum interference colours range to upper second order and extinction is parallel, or nearly so, to the length of the plates in the bundles.  All views are 5.5 mm across.  A, C ppl, B, D x-nicols.

15. Chlorite, trioctahedral - Mg3Si4O10(OH)2.Mg3(OH)6
Plane-Polarized Light
Low relief, colorless to green. Light green is most common shade.
Micaceous cleavage
Crossed Polarizers
Low birefringence results in first-order whites. Anomalous interference colors very common (A). Dark blue, brown, purple and green are possible.
Fine-grained varieties often show undulose extinction.

16. General occurrence A. alteration product of ferromagnesian minerals
B. low-grade metamorphic rocks

17. A. alteration product Chlorite after biotite
Small residual brownish patches
of biotite still occur
low first order,
anomalous Berlin
blue interference color
= Fe-rich chlorite

18. B. low-grade metamorphic rocks