Transcript Lecture 11 Structural Geology

Lecture 11 Structural Geology
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Rock deformation and structural geology
Folds in Rock
Rock fractures: Joints and Faults
Geologic maps
• Rock deformation and structural geology
 Rocks deform under stress. Deformation refers to all changes in
volume and/or shape of a rock body.
 Structural geology examines the present state of crustal deformation
and determines the original geologic setting and the nature and
direction of the earth forces (tectonic forces) that produced these rock
structures.
 Folding in a rock occurs in the plastic range of the rock.
 Faulting occurs when the rocks break.
• Laboratory experiments of deformation of marble by
compressive forces under confining pressures similar to
shallow crust (middle) and deeper crust (right). (M.S.
Patterson).
• Deformation of A) flat-lying strata. B) compressional stress
tend to shorten a rock body, often by folding. C) Tensional
stress acts to elongate or pull apart a rock unit. D) Shear
stress acts to bend and break them. (Tarbuck and Lutgents)
• Anticlines and synclines in the Calico Hills near Barstow,
California. (Hamblin and Christiansen)
• Descriptions of an inclined plane: strike
and dip
• Strike is the direction of the line produced by the
intersection of the inclined plane with the horizontal plane.
It is expressed as the angle of the line from the north.
• Dip is the angle between the inclined plane and the
horizontal plane.
• Strike and dip directions are always mutually perpendicular.
• Strike and dip of a rock layer. (Tarbuck and Lutgents)
• Folds in Rock
A fold is a bent structure that originally was
planar, such as a sedimentary bed. Folds
may be produced by either horizontal
compression or vertical forces in the crust,
just as pushing in on opposite sides of a
paper or up from below.
• Terms used to describe the parts of a fold:
• limb: The two sides of a fold are called limbs.
• axis: A line drawn along the points of maximum curvature
of a layer of a fold. More strictly, it is called hinge line.
• axial plane: an imaginary plane surface that divides a fold
as symmetrically as possible.
• plunge: If the fold axis is not horizontal, the angle of the
axis with the horizontal plane is called plunge.
• Terms describing a fold. (Tarbuck and Lutgents)
• Types of folds
• anticline: upfolds or arches of rock layers
• syncline: downfolds or troughs of rock layers.
• monocline: only one direction of dip prevails in a fold
system.
• symmetrical fold: the axial plane is vertical with the
limbs dipping symmetrically from the axis
• asymmetrical fold: the axial plane is tilted from the
vertical with one limb dipping more steeply than the other.
• overturned fold: one limb is tilted beyond the vertical
• recumbent fold: this is an overturned fold "lying on its
side" so that the axial plane is nearly horizontal.
• An illustration of principle types of folds.
• Anticlines and synclines in the Calico Hills near Barstow,
California. (Hamblin and Christiansen)
• Folds of deformed sedimentary strata near Palmdale, California. The
dashed-line indicates a fault also present. (E.J. Tarbuck)
• (Top) The San Rafael monocline, Utah. (S. Trimble) (Bottom)
Illustration of monocline consisting of bent sedimentary beds caused
by faulting in the bedrock below.
• Overturned fold. (G.S. Of
Israel). One limb has been
turned completely upsidedown with older beds on the
top.
• A recumbent fold in Precambrian rocks of the Umanak
area, Greenland. (T.C.R. Pulvertaft)
• Outcrop (map) view of folds
• Anticline: the oldest beds are in the center and the beds
become progressively younger in each direction.
Synclines: the youngest bed is in the center and the beds get
progressively older in each direction.
• Symmetrical folds have equal bed widths on opposite sides of
the axial plane, but asymmetrical folds will have different bed
widths on the opposite sides.
• For a plunging anticline, the nose (formed by the intersection
of the fold system with a horizontal plane) points in the same
direction as the plunge. For a plunging syncline, the nose
points in the direction opposite to that of the plunge.
• The diagram shows the surface of eroded remnants of a
syncline and the characteristic core of younger rocks
flanked on both sides by older rocks dipping toward the
core. (Press and Siever)
• Anticlines and synclines. The numbers 1 through 6 indicate
strata of progressively younger ages. (West, p.203)
• Symmetrical and asymmetrical anticlines and synclines.
Symmetrical folds have equal bed widths on opposite sides
of the axial plane, but asymmetrical folds will have
different bed widths on the opposite sides. (West, p.203)
• Plunging folds. Note the nose of a plunging anticline in
outcrop points in the direction of the plunge, while the
opposite is true of plunging synclines. (Tarbuck and Lutgents)
• A plunging anticline forms a a V-shape pattern pointing in
the direction of plunge. This example is from near St.
George, Utah. (Hamblin and Christiansen)
Domes (dome-shaped folds) and basins (bowl-shaped
folds). (W.W. Norton)
• Rock fractures: Joints and Faults
• Joints
 A joint is a crack along which no appreciable movement
has occurred.
 Most joints are produced when rocks are deformed by
tectonic forces, with some exceptions.
• Eroded joints, Arches National Park, Utah. (W. Clay)
• Devil’s Tower, Wyoming. The columnar joints form when
igneous rocks cool and develop shrinkage fractures
producing elongated columns. (Thomason/Stone Images)
• Joints in granitic rocks near the top of Lembert Dome, Yosemite
National Park. The joints were enhanced by weathering. (E.J. Tarbuck)
• Faults
A fault is a fracture with relative movement
of the rocks on both sides of it, parallel to
the fracture.
Fault terminology:
strike, dip of fault plane, hanging wall,
footwall.
A fresh fault scarp after an earthquake in Nevada. (S. Marshak)
(a)
(b)
(a) Slip lineations on a fault surface. (b) Breccia, broken-up
rocks along this fault. (S. Marshak)
• The names of hanging wall and footwall came from miners
mining along fault zones, who hung their lanterns on the hanging
wall and walked on the footwall. (Tarbuck and Lutgents)
• Types of faults:
• dip-slip fault: normal fault, reverse fault,
thrust fault
• strike-slip fault: left lateral, right lateral
• oblique-slip fault: has both strike-slip and
dip-slip component. Note: The textbook
calls it "translation fault", which is rarely
used.
• Types of faults. a) Normal faults, caused by tensional forces,
result in extension. b) Reverse faults, caused by compressional
forces, result in shortening. c) Strike-slip faults associated with
shearing forces. d) Oblique slip suggests a combination of
shearing and compression/tension. (Press and Siever)
• A normal fault. (Tarbuck and Lutgents)
• A small normal fault along the road to Kolob
Terraces just north of Toquerville, Utah.
• Normal faulting in the Basin and Range Province. Tensional
stresses elongated and fractured the crust into numerous
blocks. Movement along the fractures tilted the blocks
producing parallel mountain ranges. (Tarbuck and Lutgents)
• The relative movement of a reverse fault
• The Keystone thrust fault of southern Nevada. Dark-colored limestone
(Cambrian) has been thrust over light-colored Jurassic sandstone,
younger by some 350 million years. (J.S. Shelton)
• Diagram for a strike-slip fault (right-lateral). Note how the
stream channels have been offset by fault movement. (after
R.L. Wesson et al.)
• Strike-slip faults are commonly expressed by a series of straight linear
ridges and troughs that can be traced for long distances. Here the San
Andreas fault in southern California offsets a drainage system.
• The San Andreas Fault system runs from the Gulf of
California and enters the Pacific from northern California.
The accumulated displacement, from earthquakes and
creep, exceeds 560 km over its 29-million-year history.
(Tarbuck and Lutgens)
• Geologic maps
• Geologic maps are among the best sources of
information for preliminary site location and
design. Thus, engineers need to become familiar
with the construction and use of these maps.
• Elements of a geologic map include rock types,
relative ages of the rocks, geologic contacts
between different rock units, geologic structures
(e.g., faults), and maybe topographic contours.