Silicate minerals

ISOLATED SILICATES [Nesosilicates]In this group, silicon tetrahedra share no oxygen anions with other tetrahedra, and so have an excess negative charge of 4-.. SINGLE CHAIN SILICATES [In

SILICATE MINERALS

Prepared by Dr F Clark,Department of Earth and Atmospheric

Sciences, University of Alberta

Sept 05

ISOLATED SILICATES [Nesosilicates]

In this group, silicon tetrahedra share no oxygen anions with other tetrahedra, and so have an excess negative charge of 4- In the mineral olivine, this is balanced by the insertion of a pair of divalent cations in the crystal structure, either or both of Mg2+ and Fe2+ The chemical formula for olivine is written (Mg,Fe)2SiO4, which tells us that for every silicon, there are four oxygen and two

cations, either or both of Mg and Fe This option, which illustrates ionic substitution, is indicated by separating these elements by a comma within the parentheses We have variation within fixed limits, those limits being

100% Mg and 100% Fe, or any proportion in between

Olivine exhibits its classic glassy, olive green appearance in these

specimens, as well as its common granular [somewhat like sugar]

habit There is no cleavage, only conchoidal fracture, so that there are

no plane surfaces reflecting light.

SINGLE CHAIN SILICATES [Inosilicates]

In the single chain silicates, each silicon tetrahedron shares two oxygen anions, one with one neighbouring

tetrahedron, and one with another, to produce long,

strongly bonded chains Each shared oxygen accounts

for only 1- rather than the usual 2-, so that for each

silicon tetrahedron, the excess negative charge is now

only 2-, which still requires insertion of cations in the

crystal structure These cations are bonded to, and

serve to link, the chains, but these bonds are weaker

than those within the chains The single chain silicates thus cleave parallel to the chains, along two planes that meet at approximately 90 degrees

Pyroxene [e.g augite]

In these three views of two specimens, the upper face and left side vertical face meet at right angles, a common characteristic of the

single chain silicates Note how irregular the faces are on the two images on the right, yet how these small steps are parallel to each other The hardness, around 5 ½ to 6, white streak, and typical dark colour make this otherwise very similar to amphibole, a double chain silicate The square cross-sections of pyroxene crystals distinguishes them from amphiboles.

DOUBLE CHAIN SILICATES

[Inosilicates]

As with single chain silicates, chains are constructed by

sharing of two oxygen for each silicon tetrahedron The double chains are constructed by having every second silicon along the chain share a third oxygen with a

silicon from the facing chain The net result is that on

average, each silicon shares 2 ½ oxygen, so the excess negative charge per silicon is reduced to 1 ½ Cations serve to balance charge and link the strongly

constructed double chains, whose extra width causes

the cleavage planes to change orientation and meet at approximately 60 and 120 degrees, producing hexagonal cross sections

Amphibole [e.g hornblende]

In the double chain silicates, the extra width of the double chain skews the intersection angle between cleavage faces, so that they meet to form hexagonal cross sections to the crystals, as highlighted by the

yellow lines in the right-hand image In this case, we are sighting along the length of the chains Other major properties are as for pyroxene.

SHEET SILICATES [Phyllosilicates]

In this group, each silicon tetrahedron shares three oxygen anions with neighbouring tetrahedra, so that the net

negative charge per silicon is now 1- This produces a kind of hexagonal honeycomb sheet, in which all

tetrahedra point in the same direction This enables

these layers to bond with layers of cations at the centres

of octahedra with oxygen as the apices There is great variety in the combinations that are possible However, there is an asymmetry to the charge distribution which leads to net surface charges on the sheets, which are

then weakly bonded to each other by cations This leads

to the characteristic property of this group – one perfect cleavage, parallel to the sheets

As with all mica group minerals within the sheet silicates, biotite cleaves readily to produce flexible cleavage flakes whose surface has significant reflectance, such that small flakes or crystals within a rock typically

glint It is soft as well, and not readily confused with anything else You may rely on the colour to be this consistent, almost black or very dark brown shade, to distinguish from other micas, such as muscovite.

Soft, and with flexible, highly reflective cleavage flakes, the mica group mineral muscovite is distinguished consistently and reliably from the darker cousin biotite by its clear to silvery colour Muscovite contains aluminum, whereas biotite has iron and/or magnesium in the same site

in the crystal struture, which accounts for the consistent colour

difference.

metamorphic rocks that are called greenschists.

FRAMEWORK SILICATES

[Tectosilicates]

Finally, all four oxygen are shared, each one with a

different silicon tetrahedron, which eliminates the excess negative charge, given the basic formula SiO2 (the two oxygen are in effect four ½ oxygen, each being shared) One might therefore expect the framework silicates to

be the simplest group to deal with, but complexity is

introduced in the feldspar group, as we shall soon see

Among the most common rock-forming minerals, quartz is also among the easiest to identify With a hardness of 7, it is not scratched by a knife blade, but ends up with a thin streak of metal on its surface

Most commonly it has a somewhat dull, grey glassy appearance It has

no cleavages to produce plane reflecting surfaces when incorporated in rocks (see right image), but rather exhibits conchoidal fracture Its

characteristic habit is as hexagonal prismatic crystals (see left view) with pyramid terminations, seen in the specimen under the scale bar in the left image, and in the middle image.

Feldspar Group – Potassium Feldspar

In the feldspars, we see coupled ionic substitution, rather than the simple substitution exhibited by olivine By

virtue of its size, Al3+ fits between the oxygen anions of the tetrahedra in place of Si4+ Of course, this introduces

a positive charge deficiency Statistically, either one out

of every four tetrahedra, or two out of every four

of every four tetrahedra, or two out of every four

tetrahedra, may have a silicon cation replaced by

aluminum (any more than that cannot be

accommodated by the crystal structure) In the case of potassium feldspar, one out of every four tetrahedra has aluminum, and the charge deficiency is balanced by

insertion of a potassium (K+) cation

Potassium Feldspar

The most common variety of potassium feldspar is orthoclase, number

6 on Mohs hardness scale Although it is commonly a salmon pink

colour, this is not a diagnostic feature (see plagioclase feldspar images

to confirm this point) It has two cleavages that meet at right angles,

to produce square edges as seen in these specimens Streak is white This mineral may have simple twinning, but never exhibits the multiple twinning that plagioclase feldspar may show.

Potassium Feldspar

This specimen is included to emphasize the fact that one can not say with confidence that potassium feldspar is pink, and plagioclase white, although this is often the case In the left-hand image, the upper face and lower left faces are cleavages, and in the right-hand image, the upper face and shaded lower right face are cleavages Note again that

Feldspar Group – Plagioclase Feldspar

Explanation of the plagioclase feldspars carries on from

potassium feldspar The substitution of one Al3+ for Si4+

could also be balanced by Na+ This is albite, the sodium plagioclase feldspar If we substitute two Al for Si out of every four Si, the charge deficiency of 2+ is balanced by

Ca2+, and we have anorthite The ionic radii of Na+ and

Ca2+ are almost identical, so the two freely substitute, along with Al3+ for Si4+, to produce the plagioclase

feldspar solid solution series One might expect there to

be free substitution between albite and potassium

feldspar, but because the ionic radius of potassium is

approximately 40% larger than that of sodium, such

substitution is limited to elevated temperatures

Plagioclase Feldspar

This reoriented specimen exhibits the twinning striations more clearly, parallel to the blue arrows Resembling very fine scratches, they

represent the intersection between twin planes and the upper surface

of the crystal, and are flush with that surface They are not seen on the faces marked with blue stars, because they are parallel to those faces, but could be seen on the faces highlighted by green arrows.

Plagioclase Feldspar

Twinning striations are visible on the upper surface, parallel to the red arrows Because the twin planes are parallel to the right side face in the right side image, they could not be seen there, but hypothetically could

be seen on the lower, shaded face in that image The irregularity of this fracture surface makes this most unlikely in practice.

Plagioclase Feldspar

This white specimen, with twinning striations running parallel to the red arrows, illustrates the fact that portions of the twinned crystal are not necessarily all of the same thickness, although they tended to be nearly

so in the specimens in the earlier slides Note the broad uniform band, almost 1 cm wide, sandwiched between twins whose planes are less