![]() ![]() The Pacific Plate is almost entirely oceanic, but it does include the part of California west of the San Andreas Fault. Similarly the South American Plate extends across the western part of the southern Atlantic Ocean, while the European and African plates each include part of the eastern Atlantic Ocean. For example, the North American Plate includes most of North America, plus half of the northern Atlantic Ocean. The fact that the plates include both crustal material and lithospheric mantle material makes it possible for a single plate to be made up of both oceanic and continental crust. Īt spreading centres, the lithospheric mantle may be very thin because the upward convective motion of hot mantle material generates temperatures that are too high for the existence of a significant thickness of rigid lithosphere (Figure 10.12). Tectonic plates consist of lithosphere, which includes the crust and the lithospheric (rigid) part of the mantle. It is assumed that the relative lack of strength of the partial melting zone facilitates the sliding of the lithospheric plates. Plates are thought to move along the lithosphere-asthenosphere boundary, as the asthenosphere is the zone of partial melting. The plates are made up of crust and the lithospheric part of the mantle (Figure 10.17), and even though they are moving all the time, and in different directions, there is never a significant amount of space between them. Before we talk about processes at plate boundaries, it’s important to point out that there are never gaps between plates. The North American Plate, for example, rotates counter-clockwise the Eurasian Plate rotates clockwise.īoundaries between the plates are of three types: divergent (i.e., moving apart), convergent (i.e., moving together), and transform (moving side by side). The explanation is that plates move in a rotational manner. Plates move as rigid bodies, so it may seem surprising that the North American Plate can be moving at different rates in different places. The North American Plate is one of the slowest, averaging around 1 cm/y in the south up to almost 4 cm/y in the north. The Pacific Plate is the fastest at over 10 cm/y in some areas, followed by the Australian and Nazca Plates. Rates of motions of the major plates range from less than 1 cm/y to over 10 cm/y. Figure 10.16 A map showing 15 of the Earth’s tectonic plates and the approximate rates and directions of plate motions. For example the Juan de Fuca Plate is actually three separate plates (Gorda, Juan de Fuca, and Explorer) that all move in the same general direction but at slightly different rates. There are also numerous small plates (e.g., Juan de Fuca, Nazca, Scotia, Philippine, Caribbean), and many very small plates or sub-plates. The major plates are Eurasia, Pacific, India, Australia, North America, South America, Africa, and Antarctic. By the end of 1967, Earth’s surface had been mapped into a series of plates (Figure 10.16). Seismic tomography reveals pieces of lithosphere that have broken off during convergence.10.4 Plates, Plate Motions, and Plate-Boundary ProcessesĬontinental drift and sea-floor spreading became widely accepted around 1965 as more and more geologists started thinking in these terms. ![]() It is likely that the plate may break along the boundary of continental and oceanic crust. In some instances, initial convergence with another plate will destroy oceanic lithosphere, leading to convergence of two continental plates. Some lithospheric plates consist of both continental and oceanic lithosphere. ![]() Both dehydration and partial melting occurs along the 1,000 ☌ (1,830 ☏) isotherm, generally at depths of 65 to 130 km (40 to 81 mi). ![]() This releases water into the hotter asthenosphere, which leads to partial melting of asthenosphere and volcanism. As the relatively cool subducting slab sinks deeper into the mantle, it is heated, causing hydrous minerals to break down. The force of gravity helps drive the subducting slab into the mantle. Subduction begins when this dense crust converges with less dense crust. As this new crust is pushed away from the spreading center by the formation of newer crust, it cools, thins, and becomes denser. These convection cells bring hot mantle material to the surface along spreading centers creating new crust. Convection cells are the result of heat generated by the radioactive decay of elements in the mantle escaping to the surface and the return of cool materials from the surface to the mantle. Plate tectonics is driven by convection cells in the mantle. Region of active deformation between colliding tectonic plates Simplified diagram of a convergent boundary ![]()
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