Chapter 5
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Transcript of Chapter 5
CHAPTER 5Crystal growth and aggregation
Nucleation (growth) of crystals Mostly homogenous crystallization from melt or solution In some cases nucleation on various substrates
Epitaxy (a)○ New mineral overgrowths certain faces and edges of a substrate crystal○ Orientation of new mineral controlled by crystal structure of substrate
Topotaxy (b)○ New minerals grow on a specific surface such as a fissure vein○ Orientation of new mineral controlled by orientation relative to the contact surface
Nucleation of crystals Nuclei – starting point of crystals Grow further into various crystal morphologies:
Combination of crystal forms and aggregation Crystals can be:
Euhedral - perfect polyhedral surfaces- regular and characteristic interfacial angles- in free-space: solution or melt (phenocrysts)- or replacing pre-existing minerals in metamorphic rocks (porhyroblasts)
Anhedral - irregular surfaces- in most rocks
Crystal habit Def: Typical external appearance of a mineral, its combination
of crystal forms, and the relative development of these forms
Morphologies mostly not perfect polyhedra
Many minerals have, however, a characteristic shape which is useful for identification Equant or equiaxed Elongated (columnar, prismatic, acicular, fibrous, hair-like) Flattened (platy or tabular)
Can be observed in hand specimens and thin sections as the typical form in which a mineral crystallizes
Crystal habit
Habit Crystal form depends on growth history
If growth velocities remain constant with time, the original morphology is preserved
Commonly growth velocities change with timeThis can be seen best in thin sections of
minerals displaying zoning or sector zoning
Twinning
Defintion: Intergrowths where host and twin are sharing a lattice plane (twin plane) or lattice direction (twin axis)
During normal growth of a crystal, lattice layers are added to the crystal face in same orientation as previous ones
In some cases, however, layers added in ‘wrong’ orientation
Twinning begins in most instances when crystals are very small. An ion in the growing crystal may take a position which is not geometrically perfect. If rapid growth takes place, it is possible for this ion to serve as a seed attractive to arriving ions
which attach themselves and establish a new direction of growth. Gradually, the offset crystal enlarges and becomes half of the twin.
Since twinning occurs early, it is usual to find twin parts nearly, if not exactly, the same size and exhibiting the same faces, markings, etch pits etc.
Fast growth promotes twinning and conversely slow growth discourages twinning because ions have more time to shift to correct positions.
Types of twinning Penetration Twins
Share a lattice direction (twin axis) or lattice point (twin center). Have an irregular composition surface separating the individual crystals Shown here is a twinned crystal of orthoclase twinned on the Carlsbad Law with [001] as the
twin axis.
Contact Twins Share a lattice plane (twin plane or composition plane). These are usually defined by a twin law that expresses a twin plane (i.e. an added mirror
plane). The example shown here is a crystal of the mineral gypsum with a contact twin on {100}
○ Swallow Tail Twin
Contact twins can also occur as repeated or multiple twins. ○ Polysynthetic twins:○ The multiple composition planes are parallel to one another. Plagioclase commonly shows this
type of twinning, called the Albite Twin Law, with {010} as the twin plane. Such twinning is one of the most diagnostic features of plagioclase.
○ Cyclical twins:○ If the composition surfaces are not parallel to one another, but related by rotational symmetry,
they are called cyclical twins.○ Shown here is the cyclical twin that occurs in chrysoberyl along a {031} plane.
Twinning
Origin of Twinning Twinning can originate in 3 different ways:
Growth Twins○ When accidents occur during crystal growth and a new crystal is added to the
face of an already existing crystal, twinning can occur The new crystal has to share lattice points on the face of the existing crystal But has an orientation different from the original crystal.
Transformation Twins○ Transformation twinning occurs when a preexisting crystal undergoes a
transformation due to a change in pressure or temperature. This commonly occurs in minerals that have different crystal structures and different
symmetry at different temperatures or pressures. When the temperature or pressure is changed to that where a new crystal structure and
symmetry is stable, different parts of the crystal become arranged in different symmetrical orientations, and thus form an intergrowth of one or more crystals. Dauphiné and Brazil twinning in quartz commonly forms this way during a decrease in temperature.
Deformation Twins○ During deformation atoms can be pushed out of place. If this happens to produce
a symmetrical arrangement, it produces deformation twins. The mineral calcite can be easily twinned in this way, producing polysynthetic twins on {012}.
Common twinning lawsIsometric System Spinel Law
{īī1} - is a twin plane, parallel to an octahedron. It occurs commonly in mineral spinel (MgAl2O4).
Fluorite penetration twin[111] - The twin axis perpendicular to an octahedral face
adds three fold rotational symmetry. Most common in fluorite
Iron Cross [001] - The mineral pyrite (FeS2) often shows the iron
cross made of the interpenetration of two pyritohedrons.
Common twinning lawsTetragonal System Twinning in the tetragonal system
usually occurs on {011} forming cyclical contact twins.
The minerals rutile (TiO2) and cassiterite (SnO2) commonly show this type of twinning.
Common twinning lawsOrthorhombic System
Cyclical Twins {110} - The mineral aragonite (CaCO3) , chrysoberyl
(BeAl2O4), and cerrusite (PbCO3) commonly develop twinning on {110}. This results in a cyclical twin which gives these minerals a pseudo-hexagonal appearance.
Staurolite Law The mineral staurolite is really monoclinic, but it has a ß
angle very close to 90o so it has the appearance of an orthorhombic mineral. Two types of interpenetration twins occur in staurolite the {031} twins from a right-angled cross and the {231} twins form a cross at about 60o.
Common twinning lawsHexagonal System Calcite Twins
The two most common twin laws that are observed in calcite crystals are {0001} and the rhombohedron {012}. Both are contact twins, but the {012} twins can also occur as polysynthetic twins that result from deformation.
Quartz shows three other hexagonal twins. Brazil Law - {110} - is a penetration twin that results from
transformation. Dauphiné Law - [0001] - is also a penetration twin that results
from transformation. Japanese Law - {112} - is a contact twin that results from
accidents during growth.
Common twinning lawsMonoclinic System Carlsbad Law
[001] - forms a penetration twin in the mineral orthoclase. Crystals twinned under the Carlsbad Law show two intergrown crystals, one rotated 180o from the other about the [001] axis.
Swallow Tail Twins{100}- are commonly observed in the
mineral gypsum (CaSO4.2H2O).
Common twinning lawsTriclinic System The feldspar minerals plagioclase and microcline are the
most common triclinic minerals that show twinning. Two common twin laws are observed in these feldspars.
Albite Law○ Plagioclase (NaAlSi3O8 - CaAl2Si2O8) very commonly shows albite
polysynthetic twinning. ○ The twin law - {010} indicates that the twining occurs perpendicular to
the b crystallographic axis.
Pericline Law○ The pericline law has [010] as the twin axis. ○ Pericline twinning occurs as the result of monoclinic orthoclase or
sanidine transforming to microcline (all have the same chemical formula - KAlSi3O8).
○ Pericline twinning usually occurs in combination with albite twinning in microcline, but is only observable with the polarizing microscope.
Aggregation
Multicrystals, porphyroblasts and poikilocrystals
Multicrystals: slightly misoriented individual grains - Quartz quendels - Hematite roses
Repeated misorientation leads to forms such as: - Curved surfaces - Saddle morphology
Porphyroblasts : When macroscopic crystals grow and replace pre-existing minerals partialy or completely
Poikilocrystals:Crystal growing in porous rock to incorporate original rock structure (Sahara Rose – gypsum)
Growth effects Striations - tourmaline Indentations Dislocations and growth spirals – barite Dissolution (etch pits) - calcite
CHAPTER 6Isomorphism, polymorphism and crystalline defects
Isomorphism and solid solution Isomorphism:
Similar morphology (crystal forms) Different chemical composition
○ Carbonates: MgCO3 MagnesiteFeCO3 SideriteZnCO3 SmithsoniteMnCO3 RhodochrositeCaCO3 Calcite
Solid solution – a special type of isomorphism: Cations replace one another in arbitrary amounts: i.e. minerals can
have a composition that is a mixture of two pure “endmember” compositions
E.g: Olivine endmembers: Forsterite – Mg2SiO4
Fayalite – Fe2SiO4
Most olivine - (Mg, Fe)2SiO4
Also: Feldspars, Pyroxene
Polymorphism and phase transitions
PolymorphismDifferent morphology; same chemical compositionDepends on external conditionsEg. CaCO3 - Low pressure: Calcite - trigonal
- High pressure: Aragonite - orthorhombic
Undergoes phase transition:Reconstructive – bonds break – totally new structureOrder-disorder – atoms are rearranged into more ordered
configuration as T decreasesDisplacive – slight distortion of lattice – no breakage of
bonds required
Phase transitions
Crystalline defects Point defects
Vacancy or interstitial atom Dislocations (line defects)
Deformation on slip plane Planar defects
Exsolution at low TReduction in symmetry
Radiation defectsInclusions: Zircon (U and Th) in biotite
○ Haloes of different colors○ Destruction of crystal (metamictization)
Crystalline defects Point defect
Dislocations(Linear defect)
Planar defects Exsolution and ordering