Название: Earth Materials
Автор: John O'Brien
Издательство: John Wiley & Sons Limited
Жанр: География
isbn: 9781119512219
isbn:
A striking example of a modern orogenic belt is the Himalayan Mountain range formed by the collision of India with Eurasia over the past 40 Ma. The continued convergence of the Indian micro‐continent with Asia has resulted in shortening and regional uplift of the Himalayan Mountain Belt along a series of major thrust faults and produced the Tibetan Plateau. Limestones near the summit of Mt. Everest, Earth's highest mountain, were formed on the floor of the Tethys Ocean that once separated India and Asia. They were then thrust to an elevation of nearly 9 km as that ocean was closed and the Himalayan Mountain Belt formed by continental collision. The collision has produced tectonic indentation of Asia, resulting in mountain ranges that wrap around India (Figure 1.14). The Ganges River in northern India flows approximately west‐east in a trough that represents a modern foreland basin.
Continental collision inevitably produces a larger continent. It is now recognized that supercontinents such as Pangea and Rodinia were formed as the result of collisional tectonics. Collisional tectonics only requires converging plates whose leading edges are composed of lithosphere that is too buoyant to be easily subducted. In fact all the major continents display evidence of being composed of a collage of terranes that were accreted by collisional events at various times in their histories.
1.5.4 Transform plate boundaries
In order for plates to be able to move relative to one another, a third type of plate boundary is required. Transform plate boundaries are characterized by horizontal relative motion along fault systems that is parallel to the plate boundary segment that separates two plates (Figure 1.4). Because the rocks on either side slide horizontally past each other, transform fault systems are a type of strike‐slip fault system.
Figure 1.14 (a) Diagram depicting the convergence of India and Asia which closed the Tethys Sea.
Source: Courtesy of NASA;
(b) Satellite image of southern Asia showing indentation of Eurasia by India, the uplift of Himalayas and Tibetan Plateau and the mountains that “wrap around” India.
Source: From UNAVCO.
Transform faults were first envisioned by J.T. Wilson (1965) to explain the seismic activity along fracture zones in the ocean floor. Fracture zones are curvilinear zones of intensely faulted, fractured oceanic crust that are generally oriented nearly perpendicular to the ridge axis (Figure 1.15). Despite having been fractured by faulting along their entire length, earthquake activity is largely restricted to the transform portion of fracture zones that lies between offset ridge segments. Wilson (1965) reasoned that if sea floor was spreading away from two adjacent ridge segments in opposite directions, the portion of the fracture zone between the two ridge segments would be characterized by parallel relative motion in opposite directions. This would produce shear stresses that result in strike‐slip faulting of the lithosphere, frequent earthquakes and the development of a transform fault plate boundary. The exterior portion of fracture zones outside the ridge segments represents oceanic crust that was faulted and fractured when it was between ridge segments, then carried beyond the adjacent ridge segment by additional sea floor spreading. These exterior portions of fracture zones are appropriately called healed transforms or transform scars. They are no longer plate boundaries; instead, they are aseismic (lacking significant earthquakes) intraplate features because the seafloor on either side of them is spreading in the same direction (Figure 1.15). However, they do record the relative motion between two plates at the time they were actively forming.
Continental transform plate boundaries occur in continental lithosphere. The best known modern examples of continental transforms include the San Andreas Fault system in California (Figure 1.16), the Alpine Fault system in New Zealand, and the Anatolian Fault systems in Turkey and Iran. All of these are characterized by active strike‐slip fault systems of the type that characterize transform plate boundaries. In places where such faults bend or where their tips overlap, deep pull‐apart basins may develop in which thick accumulations of sedimentary rocks accumulate rapidly.
Figure 1.15 Transform faults offsetting ridge segments on the eastern Pacific Ocean floor off Central America. Arrows show directions of sea floor spreading away from the ridge. Oppositely directed arrows (black) indicate transform plate boundaries. Similarly directed arrows (red) indicate intraplate transform scars.
Source: William Haxby, with the permission of Columbia University Earth Institute; Copyright Marine Geoscience Data System.
Plates cannot simply diverge and converge; they must be able to slide past each other in opposite directions in order to move at all. Transform plate boundaries serve to accommodate this required sense of motion. Small amounts of igneous rocks form along transform plate boundaries, especially hybrid boundaries that have a component of divergence or convergence as well. They produce much smaller volumes of igneous and metamorphic rocks than are formed along divergent and convergent plate boundaries. Because they neither create nor destroy large volumes of crust/lithosphere, these boundaries are sometimes referred to as conservative plate boundaries.
Figure 1.16 Fracture zones, transform faults and ridge segments in the eastern Pacific Ocean and western North America. The San Andreas Fault system is a continental transform fault plate boundary.
Source: Courtesy of USGS.
1.6 HOTSPOTS AND MANTLE CONVECTION
Hotspots (Wilson 1963) are long‐lived areas in the mantle where anomalously large volumes of magma are generated. They occur beneath both oceanic lithosphere (e.g., Hawaii) and continental lithosphere (e.g., Yellowstone National Park, Wyoming) as well as along divergent plate boundaries (e.g., Iceland). Wilson pointed to linear seamount chains of volcanoes, such as the Hawaiian Islands (Figure 1.17), as surface expressions of hot spots, which he believed were fixed in one position for long periods. At any one time, volcanism is largely restricted to that portion of the plate that lies above the hotspot. As the plate continues to move, older volcanoes are carried away from the hotspot and new volcanoes are formed above it. As a result, the age of these seamount chains increases systematically away from the hotspot in the direction of plate motion. For the Hawaiian chain, the data suggested a west‐northwest direction of plate motion for the last 47 Ma. However, a change in orientation СКАЧАТЬ