Demonstration goals:
- Understand the effects of cooling rate on crystal size
- Understand how rapid cooling can lead to crystal fractionalization
IDEA:
When magma cools, crystals form because the solution is super-saturated with respect to some minerals. If the magma cools quickly, the crystals do not have much time to form, so they are very small. If the magma cools slowly, then the crystals have enough time to grow and become large. Some granites contain minerals which are up to one meter (3 ft) across!
Diorite with large Ca-feldspar crystal
The size of crystals in an igneous rock is an important indicator of the conditions where the rock formed. An igneous rock with large crystals probably indicates that the rock formed deep within the Earth, since it is typically warmer deep inside the Earth than near the surface. These are calledintrusiverocks, and they have aphaneritictexture (from the Greek “phanerous” meaning visible). Similarly, a rock with small crystals probably formed at or near the surface and cooled quickly. These are calledextrusiverocks and have anaphanitictexture (from the Greek “a-” meaning not, and “phanerous”). And some magma cools so quickly that no crystals form; we say that these have a hyaline texture (from the Greek “hyalis” meaning glass).
Granite with large K-feldspar crystals
Sometimes, a rock will contain both aphanitic and phaneritic crystals in it. This means that something truly odd happened to the magma before it was erupted. Since we know that large crystals need time to grow, the magma must have spent some time deep underground. But the smaller crystals mean that the rest of the cooling happened very quickly. If a rock has both crystal types, it means that the mamga spent some time in a magma chamber, where the large crystals grew, then was violently erupted onto the surface, where the small crystals were formed. A good example of this is theColbert Rhyolitein the Arbuckle Mountains of Oklahoma.
We can simulate the growth of minerals using some common materials; just about everyone has grown salt and sugar crystals from a supersaturated solution. However, those experiments take more time than is usually available in the classroom, so we have developed a demonstration based on one given inJackson, J. H., and E. D. Evans, 1980,Spaceship Earth: Earth Science, Revised Edition, Houghton Mifflin Company, p. 245-246.
To do this experiment, you will need:
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Melting the mothballs and crayon mixture | Cooling the mothballs and crayon mixture |
Before the demonstration:
Fill one beaker with 100 mL of water and place it on the hot plate; bring to a boil.
Crush one of the mothballs with the pliers and place it into a test tube; crush a crayon and add it to the test tube. Shake the test tube to mix the mothball and the crayon. Repeat, placing the other mothballs and crayons into separate test tubes. Place all three test tubes into the beaker of boiling water until the mixture melts completely.
Warning!Mothballs and crayons both give off flammable gasses when heated. Do not place the molten mixture near an open flame or spark!
1. Using tongs, place one test tube into the warm water and one into the cold water at the start of class. Begin your lecture on crystal size and morphology.
2. After about ten to fifteen minutes (depending on the temperature of the warm water), remove the test tubes from the beakers. Compare the size of the crystals. You may need to use a magnifying glass in order to see the crystals clearly; rotating the tube (to catchspecular reflection) may also help.
Do you notice anything unusual about the crystals in the tube which was placed into cold water? (HINT:Is there a color change from top to bottom of the test tube?)
For Discussion:
Why did the crystals grow to different sizes? Does crayon color have any effect on the crystal size? What about the relative amount of mothballs? Based on what you have discovered, can you explain whyice creammust be churned? (Try making ice cream without churning!)
This demonstration was adapted fromJackson, J. H., and E. D. Evans, 1980,Spaceship Earth: Earth Science, Revised Edition, Houghton Mifflin Company, p. 245-246
Related pages:
