Ch. 17 Crustal Deformation and Mountain Building

Chapter 17 Opening Figure

Rock Deformation Rock deformation refers to changes in the shape, volume, or orientation of a rock due to changes in temperature and pressure over time.

Rock Deformation due to Stress Stress is strictly defined as force per unit area, and is used to describe all forces that deform rocks Compressional stress (squeezes and shortens) Tensional stress (elongates) Shear stress (causes splaying, e.g. deck of cards).

Elastic deformation We’ve already talked about elastic deformation, which is temporary. The rock will return to original shape and form after stress is removed. What happens if the elastic limit is surpassed?

Brittle Deformation: Rocks behave like a brittle solid and fracture near surface conditions relatively low pressures and temperatures result is faulting

Ductile deformation: solid state flow of rocks that results in permanent deformation without fracture conditions at depth relatively high pressures and temperatures result is folding

Factors in Rock Deformation Pressure Temperature Rock composition Time rock is exposed to pressure and temperature

Synclines and Anticlines An anticline is a structure in which the strata (layers) in the middle are older than those of the limbs (sides). Anticlines are formed by upfolding or arching of rock layers. A syncline (“sin makes you smile”) is a structure in which the strata in the middle are younger than those of the limbs. Synclines are formed by downfolding of rock layers.

Synclines and Anticlines These two types of folds are most often found in adjacent to one another. Both are examples of ductile deformation. Both are commonly due to horizontal compressional stress.

Syncline: See the smile? Anticline Syncline: See the smile? Chapter 17, Figure 17.4

Syncline, anticline, syncline (the right syncline is cut by a vertical fault) Chapter 17, Figure 17.2a

Overturned Fold

Plunging Folds Synclines and anticlines are “plunging” when their axis is no longer parallel to the land surface, due to a perpendicular component of stress.

Plunging folds vs non-plunging folds

Monocline A monocline is a large, steplike fold in otherwise horizontal sedimentary strata Monoclines are associated with the reactivation of faults of faults in the basement rock below the sediments.

The San Rafael Swell in Utah, is an example of a monocline

Brittle Deformation: Faults Faults- fractures in rocks along which there is (or has been) displacement.

Dip-Slip Faults Movement primarily along the inclination (dip) of fault plane (i.e. up/down) Parts of a dip-slip fault Hanging wall – the rock above the fault surface Footwall – the rock below the fault surface

Normal Dip-Slip Fault Hanging wall block moves down due to gravity (that’s the normal part Associated with fault-block mountains Prevalent at spreading centers Caused by tensional forces.

Fault block mountain range produced by normal faulting Horst (high)– uplifted block, Graben (grave) – downdropped block Horst and Graben Topography: results from a series of normal faults in an extensional environment. Dip of normal faults decrease with depth. Nearly horizontal detachment fault separates brittle deformation above with ductile deformation below.

Basin and Range Geographic Province, (Nevada and parts of California, Utah)

Reverse Dip-slip Faults and Thrust Fault Hanging wall block moves up (this is the reverse of normal!) Caused by strong compressional stresses Reverse fault - dips greater than 45º Thrust fault - dips less than 45º

Thrust fault – low angle reverse fault

Thrust Fault in Nevada

What kind of fault, normal or reverse?

Strike-Slip Faults: Dominant displacement is horizontal and parallel to the trend, or strike

Strike-slip vs. Transform Strike-slip faults Dominant displacement is horizontal and parallel to the trend, or strike Often associated with tranform-fault boundaries, BUT Not all strike-slip faults are transform!

Strike-slip vs. Transform Transform fault Strike-slip fault that links spreading centers lithosphere Considered a plate boundary if large enough All transform faults are strike-slip, as they move parallel to strike.

Strike-slip faults are classified as right-lateral or left lateral Strike-slip faults are classified as right-lateral or left lateral. Which is the San Andreas?

Right-lateral or Left lateral?

San Andreas Fault System

San Andreas Fault System

From E to W, San Andreas, San Jacinto, Elsinore Faults

Peninsular Ranges Batholith and Transverse Ranges

Extension in the Basin and Range

Figure 17.20

Joints Fractures along which no appreciable displacement has occurred Most are formed when rocks in the outer-most crust are deformed

Figure 17.11

Orogenesis (Mountain Building)

Orogenesis Processes that collectively produce a mountain belt Occurs due to plate movements and often (not always!) at plate boundaries.

Orogenesis at Convergent Boundaries Island Arcs (Oceanic-oceanic crust convergence ) Subduction zone forms Volcanic arc forms Often associated with deep ocean trench

Volcanic Island Arc

Orogenesis at Convergent Boundaries Andean-type orogenesis (Oceanic-continental crust convergence ) Subduction zone forms Continental volcanic arc forms Accretionary wedge* forms seaward of arc *Large mass of sediments scraped from subducting oceanic plate which attaches to to the overiding block

Andean-Type Orogenesis

Andean-Type Orogenesis

Andean-Type Orogenesis

Andean-type orogenesis Active Examples-Volcanic Arcs Andes (accretionary wedge under water?) Cascades – active volcanoes, slightly inland from non-volcanic coastal mountains, the Olympus Range. Inactive Example: Sierra Nevada Range (magma chamber of volcanic arc) and California's Coast Ranges (accretionary wedge)

Orogenesis at convergent boundaries Accretion of Exotic Terranes Small crustal fragments collide with and accrete to continental margins Accreted crustal blocks are called terranes (note spelling). Terrane refers to any landmass that has a geologic history distinct from that of an adjoining landmass Much of western North America is composed of exotic terranes.

Accretion of Exotic Terranes

Accretion of Exotic Terranes

Accretion of Exotic Terranes

Accreted Terranes in the Western United States Source material include: island arc material (igneous parent rock) submarine deposits (sedimentary parent rock) Ancient ocean floor (igneous parent rock) displaced continental (igneous parent rock)

Orogenesis at Convergent Boundaries Collisional Mountain Belt: Two plates with continental crust converge Characterized by shortening and thickening of continental crust

Formation of Himalayas

Formation of Himalayas

Chapter 17, Figure 17.22

Collisional Mountain Ranges Active Example Himalayan Mountains and the Tibetan Plateau Inactive Example Appalachians (collision of N. America and Africa)

Figure 17.19a,b

Figure 17.19b,c

Figure 17.19c,d

Chapter 17, Figure 17.24 Landsat Image of Valley and Ridge Province, with location map on right.

Orogenesis not associated with Convergence – Fault Block Mountains Associated with Normal Faulting Basin and Range Province Teton Range, Wyoming

Isostasy The earth’s lithosphere can be thought of as “floating” in gravitational balance upon the denser, deformable rocks in the asthenosphere. To support more weight (i.e mountains) above, means you need to displace more material below.

Isostasy Horizontal compressional forces cause shortening and thickening of crust, in both directions.

Isostatic Adjustment As weight is removed from the top by erosion, the crust “rebounds” upward. The processes of erosion and isostatic uplifting will continue until mountain block reaches normal thickness. Eroded sediments cause adjacent areas to subside.

Chapter 17, Figure 17.27

Normal Fault FAULT SCARP

Reverse Fault