Minerals

Steven Dutch, Natural and Applied Sciences, University of Wisconsin - Green Bay
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Composition of Stars and Planets

Composition of the Crust

Composition of continental Crust

Eight elements make up 99 per cent of the crust. Note how rare many industrial metals are.

Minerals are the Chemicals that make up the Earth

Atomic Bonding

1. IONS

Formation of Ions

Normal Configurations: Sodium: 11 p+, e-; Chlorine: 17 p+, e-

You may have heard that the pictures above are not really accurate. If you want to know more, you can visit

What Do Atoms Really "Look Like?" (optional)

ELECTRON SHELL STRUCTURE
Most stable arrangement: 8 e- in outermost shell

2. ELECTRICAL NEUTRALITY

(+) and (-) Cancel Out

3. BONDING (SATISFY 1 & 2)

Ionic and Covalent Bonding

Ionic and Covalent Bonding

Metallic Bonding

Metallic Bonding

A. Outermost electrons wander freely through metal. Metal consists of cations held together by negatively-charged electron "glue."

B. Free electrons can move rapidly in response to electric fields, hence metals are a good conductor of electricity.

C. Free electrons can transmit kinetic energy rapidly, hence metals are good conductors of heat.

D. The layers of atoms in metal are hard to pull apart because of the electrons holding them together, hence metals are tough. But individual atoms are not held to any other specific atoms, hence atoms slip easily past one another. Thus metals are ductile. Metallic Bonding is the basis of our industrial civilization.

Hydrogen Bonding

Hydrogen Bonding

Hydrogen Bonding is Geologically Important

A. Water molecules are asymmetrical. The positively-charged portions of one are attracted to the negatively-charged parts of another. It takes a lot of energy to pull them apart. Hence:

B. The asymmetrical charge distribution on a water molecule makes it very effective in dissolving ionically-bonded materials. However, it is not an effective solvent of covalently bonded materials (oil and water don't mix). Hence:

C. When water freezes, it assumes a very open structure and actually expands. Most materials shrink when they freeze and sink in their liquid phases. Implications:

Summary of Bonding

4. LATTICE

Usually anions are bigger (They form framework and cations fill in spaces between). Thus it is often possible to remove one cation and replace it with another. Below, both halite (NaCl) and sylvite (KCl) have identical atomic structures and similar physical properties. They can be distinguished by their taste - sylvite is very bitter, somewhat like licking a belt sander. Those of you who have used so-called "light salt" know.

At right, a rubidium atom has substituted for potassium. Some elements, like rubidium, have no minerals of their own and occur in nature almost entirely by substituting for more common elements. In many minerals, this substitution occurs to such an extent that the mineral can be considered to consist of mixture of two or more ideal compounds. Such mixtures are called solid solutions.

lattice

5. RADICALS

radicals Radicals are groups of atoms that behave as single units. Three of the most common are shown at left.

NAMING MINERALS

COLOR

OTHER PROPERTIES, USES

COMPONENTS

PLACES

PEOPLE


CHEMICALS (AND MINERALS) ARE CLASSIFIED BY THEIR ANIONS

For Example: Iron Compounds Have Little in Common

On the Other Hand, Sulfides have Many Properties in Common


IDENTIFYING MINERALS


HARDNESS

Common Errors due to

MOHS vs. KNOOP Scales

  1. Talc: very small
  2. Gypsum, Fingernail: 30
  3. Calcite, Penny: 135
  4. Fluorite: 163
  5. Apatite: 430
  6. Feldspar, Glass: 560
  7. Quartz: 820
  8. Topaz: 1340
  9. Corundum: 2100
  10. Diamond: 7000

DENSITY - gm/cm3

weight relative to water

Air: 0.001
Wood - Balsa: 0.1, Pine: 0.5, Oak: 0.6-0.9
Gasoline: 0.7, Motor Oil: 0.9
Ice: 0.92
Water: 1.00
Sugar: 1.59
Halite: 2.18
Quartz: 2.65
Most Major Minerals: 2.6-3.0
Aluminum: 2.7
Pyrite, Hematite, Magnetite: 5.0
Galena: 7.5
Iron: 7.9
Copper: 9
Lead: 11.4
Mercury: 13.6
Uranium: 19
Gold: 19.3
Platinum: 21.4
Iridium: 22.4 (densest material on Earth)


MAJOR MINERAL SUITES

ELEMENTS

SULFIDES

Dense, Usually Metallic
Many Major Ores

HALIDES

Usually Soft, Often Soluble

SULFATES

Soft, Light Color

OXIDES

Often Variable, Some Ores

CARBONATES

Fizz in Acid, Give off CO2


MOST IMPORTANT MINERAL SUITE:
The Silicate Minerals

Nesosilicates - Isolated Tetrahedra

In the sketches, the O's represent oxygen atoms. The tetrahedra are viewed from above, and the Si atom would be below the central O atom. These are schematic only, the actual three-dimensional arrangement is more complex.

nesosilicates Red circles denote other cations between the tetrahedra. The silica unit behaves like any other radical. The clue to a nesosilicate is SiO4 in the chemical formula. Representatives:
-- Olivine -- Garnet -- Kyanite

Sorosilicates - Paired Tetrahedra

sorosilicates Epidote is the most common mineral of this type. The pair of tetrahedra has the formula Si2O7

Cyclosilicates - Rings

cyclosilicates Minerals with three, four, and six-sided rings are known. Examples of the rare three- and four-sided rings are at top. Six-sided rings are most common. The ring unit has the formula Si(x)O(3x) where x is the number of tetrahedra in the ring. Six sided rings thus have the formula Si6O18. The most common are:
-- Beryl (Emerald - bottom left)
-- Tourmaline (bottom right)

Inosilicates - Chains

Single Chains

pyroxenes The ratio of silicon to oxygen is 1:3, so these minerals have formulas with SiO3 or some multiple. Pyroxenes have this structure. Related minerals, called pyroxenoids, have single, but twisted, chains

Double Chains

amphiboles These minerals, the amphiboles, have Si4O11 in their formula.  A few triple-chain minerals are also known.

Phyllosilicates - Sheets

phyllosilicates These minerals have Si2O5 in their formulas. The silica sheets are sandwiched with layers of magnesium and aluminum hydroxide, water, and other cations. There are many possible structures formed by the various layering possibilities but the main groups are:
-- Micas
-- Clay minerals
-- Serpentine (asbestos) minerals

Tectosilicates - Three-Dimensional Networks

These include Quartz and the Feldspars

 

tridymite structure One of the simplest tectosilicate structures: tridymite, a high-temperature form of silica.
quartz structure Quartz has a more complex structure, with spiral chains of tetrahedra. In this diagram they are colored differently to distinguish neighboring chains.
feldspar structure The structure of the feldspars. The red atoms are potassium, sodium, or calcium. Since these atoms are cations, some of the tetrahedra contain aluminum (+3) instead of silicon (+4) to maintain charge balance.

The Problem of Crystals

Unit Cells

Repeating patterns, whether flowers on wallpaper, or atoms in a crystal, can all be described in terms of Unit Cells. A unit cell is an imaginary box that contains the basic pattern. Repeating the unit cells recreates the whole pattern. There are FIVE basic unit cells for two-dimensional patterns:

unit cells

Note that the rhombus pattern can be considered either as made up of rhombuses or as a rectangle with an extra point in the center. Crystallographers prefer the latter, because it makes the rectangular nature of the pattern clearer. Bricks in a wall have this pattern.

The hexagonal pattern can be described by rhombuses oriented in one of three ways. Two are in red and the third is outlined but not colored. The three unit cells lead to identical descriptions of the pattern.

Unit Cells in Three Dimensions

Dodecahedron

We can modify a cube by shaving off the edges, as shown in the top row. If we shave away the faces completely, the end result is a shape called a dodecahedron (Greek dodeka = twelve, hedron = side). The bottom left shows how cubic cells can be stacked to create this shape. The lower right shows the dodecahedron. In an actual crystal, the unit cells are so tiny the faces appear perfectly smooth.

Octahedron

We can modify a cube by shaving off the corners, as shown in the top row. If we shave away the corners completely, the end result is a shape called an octahedron (Greek okta = eight, hedron = side). The bottom left shows how cubic cells can be stacked to create this shape. The lower right shows the octahedron.

Below, we see some of the forms that can be made just from combining the three simple ways of stacking cubes above. Clearly, memorizing all the possible shapes is out of the question.

combining crystal shapes Animation showing how the forms below are related

combining crystal shapes

Symmetry

symmetry What crystallographers look for is the rules behind the shapes, called symmetry. All the shapes above can be cut in half in many ways to make mirror-image halves. This is called reflection symmetry

They can also be rotated in various ways to positions where they look the same as their original orientation. This is called rotational symmetry.

All together, there are 32 kinds of symmetry crystals can have, grouped into six classes according to the shapes of the unit cells in the crystal.

symmetry Animation of Symmetry

Upper Left: several possible ways of cutting the crystal into mirror-image halves are shown. There are numerous others not shown.

Upper Right: Note that the crystal looks the same four times during a complete rotation. We refer to this rotation axis as a four-fold symmetry axis.

Lower Left: The crystal looks the same three times during a complete rotation. We refer to this rotation axis as a three-fold symmetry axis.

Lower Right: The crystal looks the same twice during a complete rotation. We refer to this rotation axis as a two-fold symmetry axis.

Note (for the passionately interested only) that something irregular with no symmetry will only look the same once during a 360-degree rotation. Thus crystallographers say something with no symmetry has one-fold symmetry. It sounds convoluted, but all the mathematical formulas (yes, there is math in geology!) that are used to describe symmetry work perfectly. 

The Crystal Classes

Just as plane patterns can be described in terms of five unit cells, three dimensional patterns can be thought of as belonging to one of six classes. Just as there are two kinds of rectangular plane patterns, there are several types of three-dimensional pattern for each of the six crystal classes

isometric minerals ISOMETRIC or CUBIC
All edges equal, all angles 90 degrees
Halite, Fluorite, Pyrite
Galena, Garnet, Magnetite
Gold, Copper, Diamond
tetragonal minerals TETRAGONAL
Two edges equal, all angles 90 degrees. Square cross-section but different third dimension.
Zircon
Chalcopyrite
orthorhombic minerals ORTHORHOMBIC
No edges equal, all angles 90 degrees. Like the shape of a cereal carton.
Olivine, Andalusite, Sillimanite
Some Amphiboles and Pyroxenes
Topaz, Sulfur
monoclinic minerals MONOCLINIC
No edges equal, two angles 90 degrees. The shape obtained by knocking the ends out of a carton and skewing it.
Some Amphiboles and Pyroxenes
Micas
Gypsum, Epidote
Sugar also belongs to this crystal class.
triclinic minerals TRICLINIC
No edges equal, no angles 90 degrees
Most Feldspars
Kyanite
Clay Minerals

What if you have one 90 degree angle, or two equal edges? It turns out that these contribute no extra symmetry and the crystal is still triclinic.

hexagonal minerals HEXAGONAL 
Angles of 60, 90, and 120 degrees.
Ice (snowflakes)
Quartz, Beryl
Corundum, Hematite
Calcite, Dolomite

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Created 8 February, 1997
Last Update 23 January, 2001

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