1. EARTH SCIENCE Prentice Hall EARTH SCIENCE Tarbuck Lutgens 

3. 9 Chapter 9 Plate Tectonics Iceland: the mid-ocean ridge above ground!

4. 9.1 Continental Drift  Wegener’s continental drift hypothesis stated that the continents had once been joined to form a single supercontinent. Wegener proposed that the supercontinent, Pangaea (meaning “all land”), began to break apart 200 million years ago and form the present landmasses. Continental Drift: http://glencoe.mcgraw- hill.com/sites/0078746361/student_view 0/unit5/chapter17/concepts_in_motion. html

5. Breakup of Pangaea

6. An Idea Before Its Time 9.1 Continental Drift  Evidence The Continental Puzzle Matching Fossils -Fossil evidence for continental drift includes several fossil organisms found on different landmasses. -Mesosaurus fossils are limited to E. So. America & So. Africa ~ so were they joined? -Land Bridges was an accepted explanation (p.249)

7. Mesosaurus

8. An Idea Before Its Time 9.1 Continental Drift  Evidence Ancient Climates – glacial deposits that match up & tropical swamps that match coal fields. Rock Types and Structures - Rock evidence for continental exists in the form of several mountain belts that end at one coastline, only to reappear on a landmass across the ocean. - Appalachian Mntns. & Caledonian Mntns. (North of Scandinavia)

9. Matching Mountain Ranges

10. Glacier Evidence

11. Rejecting the Hypothesis 9.1 Continental Drift  A New Theory Emerges Wegener could not provide an explanation of exactly what made the continents move. He suggested the tidal influence of the moon be strong enough BUT that would stop the Earth’s rotation (252). New technology (SONAR) lead to findings (Mid-Oceanic Ridge) which then lead to a new theory called plate tectonics. (Continental Drift in Action! Open hyperlink… ) Continental Drift

13. Earth’s Major Roles 9.2 Plate Tectonics  According to the plate tectonics theory, the uppermost mantle, along with the overlying crust, behaves as a strong, rigid layer. This layer is known as the lithosphere. A plate is one of numerous rigid sections of the lithosphere that move as a unit over the material of the asthenosphere. A deep-ocean trench is a long, curved valley along the edge of an ocean basin (Mariana’s)

14. Mid-ocean Ridge Lava (basalt rock)

15. Mid-Ocean Ridges Earth’s mid-oceanic ridge system forms the longest feature on Earth’s surface. In the process of Sea-Floor Spreading, new ocean floor forms along Earth’s mid- ocean ridges, then slowly moves outward across the ocean floor and finally sinks back into the mantle at a subduction zone (257). All these processes are driven by the energy of convection in the mantle.

16. http://glencoe.m cgraw- hill.com/sites/00 78746361/studen t_view0/unit5/ch apter17/concepts _in_motion.html Seafloor Spreading:

17. Evidence Iron-rich mineral grains are magnetized in the same direction as the existing magnetic field (paleomagnetism). (258) Magnetometers reveal a pattern of alternating strips of magnetized rock. These matching strips are evidence for sea-floor spreading. Shallow focus earthquakes occur in & around a trench. The deeper it is, the farther from the trench (259) Wadati-Benioff Zones are related to sea-floor spreading. The ocean floor is youngest along the mid-ocean ridge (260) and oldest… where?

19. Evidence for Plate Tectonics 9.2 Mechanisms of Plate Tectonics  Earthquake Patterns Scientists found a close link between deep-focus earthquakes and ocean trenches (Wadati-Benioff Zones). The absence of deep-focus earthquakes along the oceanic ridge system was shown to be consistent with the new theory.

22. Evidence for Plate Tectonics 9.2 Plate Tectonics  Paleomagnetism is the natural remnant magnetism in rock bodies; this permanent magnetization acquired by rock can be used to determine the location of the magnetic poles at the time the rock became magnetized. Normal polarity—when rocks show the same magnetism as the present magnetism field Reverse polarity—when rocks show the opposite magnetism as the present magnetism field

23. Polarity of the Ocean Crust

24. Evidence for Plate Tectonics 9.3 Plate Tectonics  The lithosphere is broken into plates.  They are generally oceanic and continental lithosphere moving about 5 cm per year (261).  Sea-floor spreading begins at divergent boundaries, new lithosphere is produced at constructive plate margins.  Rift Valleys = Rhine Valley & East Africa which could become a narrow sea (264, Fig 16 C)

25. Paleomagnetism Preserved in Lava Flows

26. Convergent Boundaries 9.3 Plate Tectonics Lithosphere is “destroyed” at these as the leading edge of one is bent downward to slide beneath the other and subducted into the mantle (265). Fig. 266 Continental lithosphere cannot be subducted, b/c it floats ~ continental- continental convergence forms mntn. ranges ~ when India rammed into Asia (267) Continental Transform Fault = San Andreas (268) = Strike-slip fault.

27. Wadati – Benioff Zone

28. Types of Plate Boundaries 9.2 Plate Tectonics  Divergent boundaries (also called spreading centers) are the place where two plates move apart.  Convergent boundaries form where two plates move together.  Transform fault boundaries are margins where two plates grind past each other without the production or destruction of the lithosphere.

29. Three Types of Plate Boundaries

30. Divergent Boundaries 9.3 Actions at Plate Boundaries  Oceanic Ridges and Seafloor Spreading Oceanic ridges are continuous elevated zones on the floor of all major ocean basins. The rifts at the crest of ridges represent divergent plate boundaries. Rift valleys are deep faulted structures found along the axes of divergent plate boundaries. They can develop on the seafloor or on land. Seafloor spreading produces new oceanic lithosphere.

31. Spreading Center

32. Divergent Boundaries 9.3 Actions at Plate Boundaries  Continental Rifts When spreading centers develop within a continent, the landmass may split into two or more smaller segments, forming a rift.

34. East African Rift Valley

35. Convergent Boundaries 9.3 Actions at Plate Boundaries  A subduction zone occurs when one oceanic plate is forced down into the mantle beneath a second plate. Denser oceanic slab sinks into the asthenosphere.  Oceanic-Continental Pockets of magma develop and rise. Continental volcanic arcs form in part by volcanic activity caused by the subduction of oceanic lithosphere beneath a continent. Examples include the Andes, Cascades, and the Sierra Nevadas.

36. Oceanic-Continental Convergent Boundary Fig. 17 ~ on the test!

37. Convergent Boundaries 9.3 Actions at Plate Boundaries Two oceanic slabs converge and one descends beneath the other.  Oceanic-Oceanic This kind of boundary often forms volcanoes on the ocean floor. Volcanic island arcs form as volcanoes emerge from the sea. Examples include the Aleutian, Mariana, and Tonga islands.

38. Oceanic-Oceanic Convergent Boundary Wadati – Benioff Zones

39. Convergent Boundaries 9.3 Actions at Plate Boundaries When subducting plates contain continental material, two continents collide.  Continental-Continental This kind of boundary can produce new mountain ranges, such as the Himalayas.

40. Continental-Continental Convergent Boundary

41. Collision of India and Asia

42. Transform Fault Boundaries 9.3 Actions at Plate Boundaries  At a transform fault boundary, plates grind past each other without destroying the lithosphere.  Transform faults Most join two segments of a mid-ocean ridge. At the time of formation, they roughly parallel the direction of plate movement. They aid the movement of oceanic crustal material.

43. Transform Fault Boundary

44. The San Andreas Fault (a transform fault).

45. Causes of Plate Motion 9.4 Mechanisms of Plate Motion  Scientists generally agree that convection occurring in the mantle is the basic driving force for plate movement. Convective flow is the motion of matter resulting from changes in temperature (warm matter rises & cold matter sinks).

47. 9.5 Mechanisms of Plate Motion Ridge-push: As oceanic crust moves away from a divergent boundary and cools, it becomes denser and sinks compared to the newer, less-dense oceanic crust. As the cooler, denser crust sinks, the “push” of the rising crust at the boundary is thought to “push” the oceanic plate toward the trench. It contributes somewhat to plate motion. Slab-pull is a mechanism that contributes to plate motion in which cool, dense oceanic crust sinks into the mantle and the weight of this plate “pulls” the trailing slab of lithosphere down into the mantle like a tablecloth slipping off a table will pull dishes off with it. It is thought to be the primary downward arm of convective flow in the mantle.

49. Causes of Plate Motion 9.5 Mechanisms of Plate Motion  Mantle Convection The unequal distribution of heat within Earth causes the thermal convection in the mantle that ultimately drives plate motion. Mantle plumes are masses of hotter-than- normal mantle material that ascend toward the surface, where they may lead to igneous activity.

50. Mantle Convection Models

51. The End!!