Mountain building1
Upcoming SlideShare
Loading in...5

Mountain building1






Total Views
Views on SlideShare
Embed Views



1 Embed 2 2


Upload Details

Uploaded via as Microsoft PowerPoint

Usage Rights

© All Rights Reserved

Report content

Flagged as inappropriate Flag as inappropriate
Flag as inappropriate

Select your reason for flagging this presentation as inappropriate.

  • Full Name Full Name Comment goes here.
    Are you sure you want to
    Your message goes here
Post Comment
Edit your comment

    Mountain building1 Mountain building1 Presentation Transcript

    • Cotopaxi Volcano in Ecuador
    • Cotopaxi
      • Deformation – refers of all changes in the original shape or size of a rock body.
      • Brittle deformation – at the earth’s surface, low temperatures and low pressures, solid rock fractures
      • Ductile deformation – deep with in the Earth, high temperatures and high pressures, rock is deformed without breaking
      • The mineral composition and texture also affects how it will deform.
      • Small stresses applied over time will cause the rock to bend.
      • Stress – force per unit area acting on a solid
      • Strain – the change in shape or volume
      • Tensional stress – causes a material to be stretched
      • Compressional stress – causes a material to shorten
      • Shear stress – causes a material to be distorted
      • Folds – during mountain building flat-lying sedimentary and igneous rock are bent into a series of ripples
      • Anticlines – arching of rock layers
      • Synclines – downfolds or troughs
      • Monoclines – large step-like folds
      • Faults – fractures in the crust along which movement has taken place
      • Normal fault – when the hanging wall block moves down relative to the footwall block, caused by tensional forces
      • Reverse fault – the hanging wall block moves up relative to the footwall, caused by compressional forces
      • Thrust faults – reverse faults with dips less than 45o
      • Strike-slip faults – the movement is horizontal and parallel, caused by shear stress, San Andreas fault
      • Joints – most common rock structure, fractures along which no appreciable movement has occurred
      • Mountains – classified by the dominant processes that deformed them
      • Folded Mountains – formed by folding, compressional stress is the major force that formed them; examples – Appalachians, Alps, northern Rocky Mountains
      • Fault-block Mountains – mountains that form as large blocks of crust are uplifted and tilted along normal faults; examples – Tetons Range, Sierra Nevadas
      • Horst and Grabens – formed from tensional forces, horsts are uplifted structures and grabens is where the blocks dropped down; example – the Basin and Range region of Nevada, California and Utah
      • Domes – formed by upwarping and exposing older igneous and metamorphic rock; example – Back Hills of South Dakota
      • Basins – downwarping structures having a circular shape
    • Mountain Building – Orogenesis
      • Mountain Building at Convergent Boundaries – colliding plates provide the compressional forces that deform rock
      • Oceanic-Oceanic Convergence – forms volcanic island arcs, Aleutian Islands of Alaska
      • Ocean- Continental Convergence – ocean crust subducts the continental crust, the continental crust is deformed, creates volcanic arcs on continent
      • Accretionary wedge – accumulation of different sedimentary and metamorphic rocks
      • Continent-Continent Convergence – form folded mountains; examples – Himalayas, Ural mountains
      • Mountain Building at Divergent Boundaries – fault-block mountains
      • Non-Boundary Mountains – Hawaiian Islands are volcanic islands formed by a hot spot
      • Continental Accretion – smaller crustal fragments collide and merge with continental margins; example – many of mountains rimming the Pacific Canada and Alaska
      • Terranes – any crustal fragment that has a geologic history distinct from adjoining terranes
      • Isostacy – a floating crust in gravitational balance. As mountains erode, the crust rises in response to the reduced load. Erosion and uplift continue until the mountains reach normal crustal thickness
      • The weight of the ice sheet during the Pleistocene depressed the Earth’s crust hundreds of meters. Since the ice age, uplift has occurred