2Ocean Drilling Vessel JOIDES Resolution. Fig. 7.1Ocean Drilling Vessel JOIDES Resolution.This scientific drilling ship is equippped to drill 5 miles below the ocean surface. To date, it has drilled over 500 wells worldwide. Together with its earlier sistership, the Glomar Challenger, they have drilled over 1500 wells.
3Mountain Building and Drifting Continents: Major Concepts By end of 1857 (“Heroic Age”) models of Earth all assumed that continents were fixed in place.Attempts were made to explain mountains by crustal cooling and contraction of Earth.However, even then evidence existed that the continents had moved. By 1950, submarine data had beg;un to show astonishing sea floor features. This eventually lead to “sea floor spreading” and “plate tectonics”, the crowning jewels of geologic thought.
4Fig. 7.2Early (1840) depiction of a cross-section across the Applachian Mountains. Section is across Pennsylvania from northwest (top) to southeast (bottom)
5Fig. 7.3Early theories of mountain building based largely on geologic observations in the U.S. Appalachian Mountains.A. Hall(1857) postulated that sedimentation depressed the crust at continental margins.B. Dana (1873) postulated that the crust underwent bending as the interior cooled and shrank.
6Fig. 7.4Two different interpretations of the structure of the Jura Mountains (Switzerland).Top - upper rocks slip along “basement” along a flat shear surface. (“Thin-skinned” tectonics.)Bottom - Basement rocks are involved in folding and faulting along steep (thrust) faults. (“Thick-skinned” tectonics)
7Fig. 7.5Early conception of continental drift (Arthur Holmes, 1910) showing formation of Cenozoic mountains.
8Fig. 7.6Early attempt to fit continents together by “cutting” present-day globe and rotating and squeezing islands and peninsulas. (Baker, 1912, Michigan Academy of Sciences)
9Fig. 7.7Alfred Wegener’s famous reconstruction showing three stages of continental drift. (Wegener, 1929)
10Fig. 7.8Wegener’s reconstruction of Permian continents and paleoclimate zones based on rock assemblages (glacial striations) and paleoclimate data (salt deposits, fossil ferns, etc.).
11Fig. 7.9Holmes convection current mechanism for continental drift. (A. Holmes, 1928, Physical Geology)
12Fig. 7.10A. Example of remnant magnetism with respect to present field for two rocks of different ages.B. Restoration of Cambrian magnetic field after correcting for post-Cambrian folding.
14How do we reconstruct paleo continental positions? Early pioneers had to use geology (glacial striations, salt deposits), paleontology (fossils) and geometryBut all this changed when paleomagnetism was discovered and used to recreate positions of continents in the past.
15Fig. 7.11Schematic representation of components of fossil magnetism. The declination angle provides information on paleolongitude. The inclination angle provides information on paleslatitude. With paleo-lat-long coordinates and the age of the rock, its position on the Earth can be plotted.
16Relationship of earth’s magnetic field to remanent magnetism in rocks. Fig. 7.12Relationship of earth’s magnetic field to remanent magnetism in rocks.I. PresentII. Present discordant (measured) positionsIII. Restored positions (paleogeographic locations)
20Fig. 7.13Different positions of North America relative to the equator from Cambrian time to present. Note progressive counterclockwise rotation and northward drift throughout time.
21Fig. 7.14Restoration of continental positions of longitude in the past using paleomagnetic data. The declination angle of a sample points toward the paleomagnetic pole. Continental positions must be adjusted until ancient pole positions for two continents coincide. Having outline for original continental margins helps.
22Fig. 7.18The East African rift system showing the Afar Triangle as a triple-junction at the intersection of the Red Sea, Aden and East African rifts. Possibly the expression of a mantle plume. Diverging rifts starts a new round of continental drifting and ultimately “creates” new ocean floor. Dots indicate young volcanoes.
24Prior to the 1960’s most geologists considered the ocean floors to be generally featureless plains, the oceanic crust to be very old and topographically featureless. It was also assumed to be fixed in place. By 1970, all this had changed.
25Fig. 7.19Model for sea-floor spreading showing expansion of ocean ridges (divergent) and arc-trench (convergent) systems. Three lithospheric plates are shown moving over the weak low-velocity zone of the upper mantle. Magmas are produced in arcs by heating along the subduction zone. Deep earthquakes are concentrated in the relatively cool, brittle downgoing slab. Shallower earthquakes occur under the spreading ridges. The 1000 C contour illustrates the contrast between hot upper mantle beneath ridges and cooler region beneath the arcs.
26Gemini spacecraft photo of Gulf of Aden and southern Red Sea Fig. 7.20Gemini spacecraft photo of Gulf of Aden and southern Red Sea
27Fig. 7.21Comparison of motion on transform and transcurrent (strike-slip) faults. Red lines are spreading ridge axes. A and B show two different stages for each case.Upper: Plates are spreading away from ridge axis and the transform fault connects two offset segments of that axis. Segments of adjacent moving oceanic crust slide past one another along the transform while spreading occurs.Lower: Sea-floor spreading ceased before A and then a transcurrent fault cut the ridge. Between times A and B the dead ridge was offset in the direction shown by the arrows in the opposite sense of displacement from that of the transform fault.
29Lithospheric plates (A, B, C) move (rotate) around an imaginary pole. Fig. 7.22Geometry of spreading ridge axis, transform faults and subduction zonesLithospheric plates (A, B, C) move (rotate) around an imaginary pole.Transform faults are perpendicular to the spreading axis (parallel to imaginary lines if latitude around the rotation pole.Rates of spreading are indicated by lenghs of arrows and increase from rotation pole to (rotation) equator.
33Paleomagnetism helps date age of oceanic crust. Fig. 7.26Paleomagnetism helps date age of oceanic crust.
34Earthquake epicenters 1961-1967 Fig. 7.27Earthquake epicentersNote how epicenters outline plate boundaries. Arrows indicate direction of horizontal motion during earthquakes.
35Major Lithospheric Plates Fig. 7.28Major Lithospheric PlatesPlates as defined by seismicity (previous slide). Arrows show direction of plate motion and confirm hypothesis of sea-floor spreading by showing divergence (extension) away from ocean ridges and convergence (compression) toward volcanic arc-trench (subduction) zones.
36Possible Driving Mechanisms for Plate Tectonics Fig. 7.30Possible Driving Mechanisms for Plate Tectonics1. Ocean ridge push2. Gravity sliding (down slope of an ocean ridge)3. Gravitational pull on a cold plate (down a subduction zone)4. Carried on convection cell.
37Types of Plate Interactions Fig. 7.31Types of Plate Interactions
38The Six Major Types of Sedimentary Basins Fig. 7.32The Six Major Types of Sedimentary BasinsIndonesiaNevadaE. AfricaOffshore Calif.Michigan BasinE. Coast NAThe six major types of sedimentary basins are shown in their plate-tectonic settings. The major physical cause or causes of subsidence for each case are shown below the diagram. Some examples are indicated in top.
39Stages in the Development of a Passive Margin Fig. 7.33Stages in the Development of a Passive MarginHow did we get from B to C?
40Detailed Cross-section of a Passive Margin Fig. 7.34Detailed Cross-section of a Passive MarginCretaceous & Cenozoic sedimentsAtlantic MarginJurassic saltWhat is the relativeage of the basalt?Triassic rift valley sediments
41Regional Crustal Subsidence due to local sediment loading Fig. 7.35Regional Crustal Subsidence due to local sediment loadingExample: Gulf of Mexico and Mississippi RiverSediments delivered by major river systems eventually deposit a non-negligible load on the crust, resulting in slight deformation (subsidence) and opens accomodation space for further sediment loading. (positive feedback).
42Formation of an intercratonic basin and a foreland basin Fig. 7.36Formation of an intercratonic basin and a foreland basinFormation of an intercratonic basin and a foreland basin and an intervening arch by “thrust loading” e.g thrust faulting a package of rock onto a continental margin.
43Conversion of a passive margin to a convergent margin Fig. 7.37Conversion of a passive margin to a convergent marginA classic passive margin (A) can be converted into an active convergent margin by collision with an arc (B).Thrust loading and erosion of mountains produce a foreland basin (FB).Cessation of tectonic activity and deep erosion can produce a new passive margin (C).