© 2006 pearson prentice hall lecture outlines powerpoint chapter 10 earth science 11e...
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© 2006 Pearson Prentice Hall
Lecture Outlines PowerPoint
Chapter 10
Earth Science 11e
Tarbuck/Lutgens
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Mountain Building
Chapter 10
Earth Science, 11e
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Deformation
Deformation is a general term that refers to all changes in the original form and/or size of a rock body
Most crustal deformation occurs along plate margins
Factors that influence the strength of a rock• Temperature and confining pressure • Rock type • Time
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Folds
Rocks bent into a series of wavesMost folds result from compressional forces
which shorten and thicken the crust Types of folds
• Anticline – upfolded, or arched, rock layers • Syncline – downfolded rock layers
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Folds
Types of folds • Anticlines and synclines can be
Symmetrical - limbs are mirror images Asymmetrical - limbs are not mirror images Overturned - one limb is tilted beyond the vertical
• Where folds die out they are said to be plunging
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A series of anticlines and synclines
Figure 10.3
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Plunging folds
Figure 10.5 A
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Outcrop patterns of plunging folds
Figure 10.5 A
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Folds
Types of folds • Other types of folds
Dome• Circular, or slightly elongated • Upwarped displacement of rocks • Oldest rocks in core
Basin • Circular, or slightly elongated • Downwarped displacement of rocks • Youngest rocks in core
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The Black Hills of South Dakota are a large dome
Figure 10.8
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The bedrock geology of the Michigan Basin
Figure 10.9
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Faults
Faults are fractures (breaks) in rocks along which appreciable displacement has taken place
Types of faults • Dip-slip fault
Movement along the inclination (dip) of fault plane Parts of a dip-slip fault
• Hanging wall – the rock above the fault surface
• Footwall – the rock below the fault surface
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Concept of hanging wall and footwall along a fault
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Faults
Types of faults • Dip-slip fault
Types of dip-slip faults• Normal fault
• Hanging wall block moves down • Associated with fault-block mountains • Prevalent at spreading centers • Caused by tensional forces
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A normal fault
Figure 10.12 A
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Fault block mountains produced by normal faulting
Figure 10.13
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Faults
Types of faults • Dip-slip fault
Types of dip-slip faults• Reverse and thrust faults
• Hanging wall block moves up• Caused by strong compressional
stresses • Reverse fault - dips greater than 45º • Thrust fault - dips less than 45º
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A reverse fault
Figure 10.12 B
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A thrust fault
Figure 10.12 C
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Faults
Types of faults • Strike-slip faults
Dominant displacement is horizontal and parallel to the trend, or strike
Transform fault• Large strike-slip fault that cuts through
the lithosphere • Often associated with plate boundaries
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A strike-slip fault
Figure 10.12 D
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Faults
Types of faults • Joints
Fractures along which no appreciable displacement has occurred
Most are formed when rocks in the outer-most crust are deformed
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Section Break
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Mountain belts
Orogenesis refers to processes that collectively produce a mountain belt
Mountain building at convergent boundaries • Most mountain building occurs at convergent
plate boundaries
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Mountain belts
Mountain building at convergent boundaries • Andean-type mountain building
Oceanic-continental crust convergence e.g. Andes Mountains Types related to the overriding plate
• Passive margins• Prior to the formation of a subduction
zone • e.g. East Coast of North America
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Mountain belts
Mountain building at convergent boundaries • Andean-type mountain building
Types related to the overriding plate • Active continental margins
• Subduction zone forms • Deformation process begins
• Continental volcanic arc forms • Accretionary wedge forms • Examples of inactive Andean-type
orogenic belts include Sierra Nevada Range and California's Coast Ranges
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Orogenesis along an Andean-type subduction zone
Figure 10.18 A
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Orogenesis along an Andean-type subduction zone
Figure 10.18 B
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Orogenesis along an Andean-type subduction zone
Figure 10.18 C
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Section Break
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Mountain belts
Mountain building at convergent boundaries • Continental collisions
Where two plates with continental crust converge e.g., India and Eurasian plate collision
• Himalayan Mountains and the Tibetan Plateau
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Formation of the Himalayas
Figure 10.22
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Section Break
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Mountain belts
Mountain building at convergent boundaries • Continental accretion
Third mechanism of mountain buildingSmall crustal fragments collide with and accrete to
continental margins Accreted crustal blocks are called terranes Occurred along the Pacific Coast
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Distribution of modern day oceanic plateaus and other submerged crustal fragments
Figure 10.19
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Accreted terranes along the western margin of North America
Figure 10.21
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Mountain belts
Buoyancy and the principle of isostasy • Evidence for crustal uplift includes wave-cut
platforms high above sea level • Reasons for crustal uplift
Not so easy to determine Isostasy
• Concept of a floating crust in gravitational balance
• When weight is removed from the crust, crustal uplifting occurs • Process is called isostatic adjustment
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The principle of isostasy
Figure 10.27
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Erosion and resulting isostatic adjustment of the crust
Figure 10.28 A
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Erosion and resulting isostatic adjustment of the crust
Figure 10.28 B
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Erosion and resulting isostatic adjustment of the crust
Figure 10.28 C
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End of Chapter 10