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Deformation
in rocks is usually manifested as faults
(planar
surfaces), folds (curviplanar surfaces), foliations,
and
lineations (lines). Near the earth's surface
(e.g. mid-ocean ridge extension, continental rifts), deformation usually
involves the formation of fractures in massive
rocks such as gabbro or granite, and fractures and
folds in laminated rocks such as sediments.
The structures are spaced and the deformation is said to be non-penetrative.
Under near surface conditions,
rocks may become crushed to form tectonic breccias
or cataclasites, whereas at greater depths
mineral grains in in course grained rocks may undergo a process of polygonization
involving the breakdown of large grains into an aggregate of smaller grains.
Where the grain size reduction takes place in shear zones, the rocks may
become extremely fine grained and take on a flow lamination. Such rocks
are known as mylonites; and relict grains
of the original rock material are called porphyroclasts.
(Note: large mineral grains that grow in a rock during metamorphism, e.g.
garnet, andalusite, staurolite, are known as porphyroblasts.)
At depth however, the mode
of deformation changes from brittle mode to
ductile,
deformation is penetrative, and the
structures formed usually involve folding and a component of shear
(flattening, change of shape). The change in mode of deformation takes
place at a depth of about 12 km. Where deformation has been sufficiently
intense to eradicate all primary structural features in the deformed rocks,
it is not uncommon to find domains varying in size from kilometres to meters
that have suffered minimal deformation. These domains are known as 'shear
pods', or in the case of the smaller examples 'tectonic
fish', and are very useful because they provide the only means of
determining the primary character (protolith)
of the deformed rocks.
Geometrically, faults and folds
can be described in terms of sets of planes and lines (lineations). Faults
are planar surfaces, whereas folds are curviplanar
surfaces. Faults commonly exhibit a linear structure in the form of elongated
grooves called slickensides, whereas the linear
element in a fold would be the locus of points of maximum curvature of
the folded surface, usually referred to as the fold
axis or hinge line. Folds are bisected by a plane of bilateral
symmetry called the axial plane (surface).
The plane normal to the fold axis is called the fold
profile, whereas planes that cut the
fold obliquely are called false
fold profiles; on such planes the amplitude of folds is exagerated.
Foliation may form under conditions of
simple shear
(shear cleavage) or of pure shear (flattening
cleavage). When both cleavages form at the same time, they are known as
C-S
cleavages. Such cleavages are useful because they can be used to determine
the sense of movement of the rock during the deformation.
The effect of pure
shear
(flattening) is to induce the crystallization of micas or chlorite with
their crystal cleavage planes parallel to the axial planes of the fold.
In this way the fold is thinned in a direction normal to the axial plane
of the fold and elongated in a direction roughly normal to the fold axis.
The parallelism of the micas is exhibited in hand specimens as a planar
fabric parallel to the axial planes of folds. The fabric is called the
rock cleavage. Minerals such as amphibole
may also grow with a preferred crystallographic orientation. If the amphibole
crystals have an acicular habit, the rock will exhibit a linear
structure.
Large folds commonly have smaller
folds on their limbs; these folds have even smaller folds, and so on. Smaller
folds on the limbs of higher order folds are called parasitic
folds, and the folds on one limb are the mirror image
of folds on the opposing limb. Similarly, the angular
relationship of the fold limb to the cleavage on one limb of a fold
is a mirror image of the relationship on the
complementary
limb. Knowing the shape of a parasitic fold or the angular relationship
of bedding and cleavage allows the structural geologist to predict the
nature of a higher order fold structure.
Folds exhibit shape differences
according to the degree of pure shear they have suffered. The difference
is best seen in the variation of layer thickness as it is traced from the
fold limb to the fold axis. In the case of folds that have not been flattened,
beds do not change thickness. They are called concentric
folds because the curved surfaces of the layers mimic concentric
circles. Folds that have been strongly flattened exhibit bed thicknesses
that increase from the limb to the axis. If the flattening is such that
adjacent surfaces are essentially similar in form (that is, they can be
superimposed one on the other) they are called similar
folds.
Word List:
faults folds foliations lineations penetrative non-penetrative
'tectonic breccias' cataclasites polygonization mylonites porphyroclasts
porphyroblasts 'shear pods' 'tectonic fish' protolith
slickensides 'fold axis' 'hinge line' 'axial planar surface'
'fold profile' 'false fold profile' 'simple shear' 'pure
shear' 'C-S cleavage' 'linear structure' 'parasitic folds'
'concentric folds' ' similar folds'
FIGURES