1. Mountain Building & rock deformation (they go together)
Chapter 11
Mountain Building & rock deformation (they go together)

2. Rock Deformation
It is theorized that all continents were once mountainous masses and grow by adding mountains to their edges.
If this is so, then how do mountains grow in the middle of continents?

3. Factors Affecting Deformation
Every rock has a point at which it will bend and/or break.
Deformation is the term that refers to all changes in the original shape and/or size of a rock body.
Most deformation occurs at plate margins.

4. Principle of Isostasy
This is a gradual up and down motion of materials that make up the interior of continents away from continental margins.
Earth’s crust floats on top of denser more flexible rocks in the mantle.
The concept of a floating crust in gravitational balance is isostasy.

5. Mountain belts float on top of more dense crustal roots that extend into the mantle.
The denser mantle supports the mountains from below.

6. If more material were added to the top of the mountains the combined block would sink until a new isostatic balance was reached.
However, the top of the combined block would be higher than before and the bottom would be lower.
This process of establishing a new level of gravitational equilibrium is called isostatic adjustment.

9. Isostatic Adjustment of Mountains
Continental ice sheets provided evidence of crustal subsidence followed by rebound.
The weight of 3 kilometers of ice depressed Earth’s crust by hundreds of meters.
In 8000 years since the last ice sheets melted, uplift of as much as 330 meters has occurred in Canada’s Hudson Bay region.

10. Most mountain building causes the crust to shorten and thicken.
Because of isostasy, deformed and thickened crust will undergo regional uplift both during mountain building and for a long period afterward.
As the crust rises (rebounds) the processes of erosion increases and the deformed rock layers are carved into mountains.

11. Erosion removes material from the summit reducing the load causing the crust to rise. This will continue until the mountain block reaches its “normal” thickness.

13. Stress is the force per unit area acting on a solid
Stress is the force per unit area acting on a solid. Under great stress, rocks tend to deform usually by:
Folding
Faulting
Flowing
Fracturing

14. Stress and Strain
The change in shape or volume of a body of rock as a result of stress is called strain.
Rocks can be bent into folds if stress is applied gradually and not going beyond the breaking point.
We already know that rocks under stress have elastic properties and will go back to their original shape and size when the force is removed. (elastic rebound)

15. Once the elastic limit or strength of a rock is surpassed, it either flows or fractures.

16. The factors that influence the strength of a rock and how it will deform include:
Temperature
Confining pressure
Rock type
Time

17. Temperature and Pressure
Rocks deform permanently two ways:
Brittle deformation
Ductile deformation

18. Rocks near the surface, where temperatures and confining pressures are low, usually behave like brittle solids and fracture once their strength is exceeded.
This type of deformation is called brittle failure or brittle deformation.
Examples: china, bones, pencils, glass

19. At depth, where temperatures and confining pressures are high, rocks show ductile behavior.
Ductile deformation is a type of solid-state flow that produces a change is size and shape of an object without fracturing the object.
Examples: modeling clay, bee’s wax, caramel candy, and most metals

20. Question ????????????
Placing a penny on a railroad track and having a train run over it, causing the penny to flatten out is an example of?
ductile deformation

21. Rock Type
The mineral composition and texture of a rock also affect how it will deform.
Granite and basalt contain minerals with strong internal molecular bonds will fracture.
Sedimentary rocks that are weakly cemented or metamorphic rocks that are foliated are more likely to deform by ductile flow.

22. Rocks that exhibit ductile flow may include:
Soft
Halite (rock salt)
Gypsum
Shale
Intermediate strength
Limestone
Schist
Marble

23. Time
Natural stress applied over a long period of time will fold rocks.
Forces that are unable to deform rock when first applied may cause rock to flow if the force is maintained over a long period of time.

24. Types of Stresses Three types of stresses rocks undergo include:
Tensional forces – rocks being pulled in opposite directions
Compressional force – rocks are squeezed and shortened
Shear stress – when a body of rock is distorted

25. Stresses

26. Folds
During mountain building, flat lying rocks (both sedimentary and igneous) are bent in wave-like ripples called folds.
Folds have sloping sides called limbs and when the limbs meet at the bend they are called hinges.

27. There are three types of folds:
Anticline – an upward fold (arch)
Syncline – a downward fold (trough)
Monocline – closely associated with faults, monoclines are large step–like folds in otherwise horizontal layers of sedimentary strata.
Prominent features of the Colorado Plateau which coves Colorado, New Mexico, Utah, and Arizona.

28. Anticline and Syncline Process

30. Circular Anticline

31. Syncline

34. Joints – fractures in rock strata where no movement has taken place
So faults are……………

36. Three types of faults Normal – caused by tensional stress
Reverse (or thrust) – caused by compressional stress
Strike-slip – commonly caused by shear stress – San Andreas Fault

37. Normal

38. Reverse or Thrust

39. Strike-Slip

40. What type of fault?
Strike-slip

41. What type of fault?
Normal

42. What type of fault?
Reverse or Thrust

45. Thrust fault

46. Types of Mountains
The collective processes that produce a mountain belt are called orogenesis.
The dominant processes that have formed them classify mountains.

47. Folded Mountains
Mountains formed primarily by folding are called folded mountains.
Thrust faults are also important in the formation of folded mountains.
These mountains are called fold and thrust belts.
Examples: Appalachian Mountains, the northern Rocky Mountains, and the Alps of Europe

49. Fault-Block Mountains
Large-scale normal faults are associated with structures called fault-block mountains.
These mountains form when large blocks of crust are uplifted and tilted along normal faults. 
Examples: Teton Range of Wyoming and the Sierra Nevada Range of California.

51. Fault block & Grabens
Normal faulting occurs when tensional stresses cause the crust to be stretched or extended.
As the crust is stretched, a block called a graben, which is bounded by normal faults, drops down.
Graben is German for ditch or trench.
Grabens produce an elongated valley bordered by relatively uplifted structures called horsts.
Examples: Basin and Range Province of Nevada, Utah, and California.

54. Rift or Grabben

55. Graben or Rift example is: Death Valley 250 ft. below sea level
Dead Sea is 1200 ft below sea level

56. Domes and Basins
These mountains are produced by broad upwarping in the basement rock deforming the overlying sedimentary strata.
A dome is when upwarping produces a circular or elongated structure or dome.

57. How are these domes uncovered?
Erosion strips away the highest portion of the sedimentary beds exposing older igneous and metamorphic rocks in the center.
The oldest rocks form the core of these mountains. 
Example: Black Hills

58. Downwarped structures having a circular shape are called basins.
These structures have gently sloping bed similar to saucers.
Basins are thought to be formed by the accumulation of sediment, whose weight caused the crust to subside.
Example: Basins of Michigan & Illinois
In the case of a basin the oldest rocks are found in the center with the youngest rocks on the flanks.

61. Mountain Formation Just how old are mountains?
Appalachians are 100s of million of years old
Himalayas are about 45 million years old… Just a youngster!

62. Mountain Building at Convergent Boundaries
Most mountain building occurs at convergent plate boundaries.
Colliding plates provide the compressional forces that fold, fault, and metamorphose the thick layers of sediment deposited on the edges of landmasses.

63. Ocean-Ocean Convergence
Converging oceanic plates result in subduction that creates magma leading to the growth of a volcanic island arc once it grows above sea level.
Examples: Aleutian Islands in Alaska, Japan,
Ocean-ocean convergence mainly produces volcanic mountains.

67. Ocean-Continental Convergence
Example: West coast of South America – the Andes Mountains
This produces a continental volcanic arc.
During subduction, sediment scraped from the subducting plate is stuck against the landward side of the trench.
This accumulation of sediment and metamorphic rock is called an accretionary wedge.

68. Ocean-continent convergence produces mountains in two roughly parallel belts.
The continental volcanic arc develops on the continental block and the accretion wedge is on the seaward belt.
The types of mountains formed by ocean-continent convergence are volcanic mountains and folded mountains.

70. Continent-Continent Convergence
A convergent boundary between two plates carrying continental crust, a collision between the continental fragments will result and form folded mountains.  
Example: Himalayan Mountains and the Tibetan Plateau, European continent collided with Asia producing the Ural Mountains in Russia.

72. Mountain Building at Divergent Boundaries
These mountains are usually formed on the ocean floor
Example: Mid-ocean ridges that extend 65,000 kilometers.
The mountains that form along ocean ridges at divergent plate boundaries are fault-block type mountains.

74. Non-Boundary Mountains
Example: Hawaiian Islands
Continental Accretion
Accretion is when small crustal fragments collide and merge with continental margins.

76. Terrane – is any coastal fragment that has a geological history distinct from that of the adjoining terranes.
Some may be no larger than volcanic islands, while other are immense, such as the entire Indian subcontinent.
Some may have been microcontinents similar to present day Madagascar.
Many others were island arcs like Japan and the Philippines.

77. All these materials add to the continent width and thickness displacing other fragments further inland.

79. Mountains of Accretion
Example: Mountains in western North America and western Canada contain rock, fossils, and structures different from the surrounding area.
These materials have been accreted (added to) the western margin of North America.