continental drift

Geol. the lateral movement of continents resulting from the motion of crustal plates. Cf. plate tectonics.

[1925-30]

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Large-scale movements of continents over the course of geologic time.

The first complete theory of continental drift was proposed in 1912 by Alfred Wegener, who postulated that a single supercontinent, which he called Pangaea, fragmented late in the Triassic Period (248–206 million years ago) and the parts began to move away from one another. He pointed to the similarity of rock strata in the Americas and Africa as evidence to support his hypothesis. Wegener's ideas were widely rejected until they were combined with Harry H. Hess's seafloor spreading hypothesis in the 1960s. The modern theory states that the Americas were joined with Europe and Africa until с 190 million years ago, when they split apart along what is now the Mid-Atlantic Ridge. Subsequent tectonic plate movements brought the continents to their present positions.

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▪ geology

      large-scale horizontal movements of continents (continent) relative to one another and to the ocean basins during one or more episodes of geologic time. This concept was an important precursor to the development of the theory of plate tectonics, which incorporates it.

      The idea of a large-scale displacement of continents has a long history. Noting the apparent fit of the bulge of eastern South America into the bight of Africa, the German naturalist Alexander von Humboldt (Humboldt, Alexander von) theorized about 1800 that the lands bordering the Atlantic Ocean had once been joined. Some 50 years later, Antonio Snider-Pellegrini, a French scientist, argued that the presence of identical fossil plants in both North American and European coal deposits could be explained if the two continents had formerly been connected, a relationship otherwise difficult to account for. In 1908 Frank B. Taylor of the United States invoked the notion of continental collision to explain the formation of some of the world's mountain ranges.

      The first truly detailed and comprehensive theory of continental drift was proposed in 1912 by Alfred Wegener (Wegener, Alfred Lothar), a German meteorologist. Bringing together a large mass of geologic and paleontological data, Wegener postulated that throughout most of geologic time there was only one continent, which he called Pangea. Late in the Triassic Period (which lasted from approximately 250 to 200 million years ago), Pangea fragmented, and the parts began to move away from one another. Westward drift of the Americas opened the Atlantic Ocean, and the Indian block drifted across the Equator to merge with Asia. In 1937 Alexander L. Du Toit, a South African geologist, modified Wegener's hypothesis by suggesting two primordial continents: Laurasia in the north and Gondwana in the south.

      Aside from the congruency of continental shelf margins across the Atlantic, modern proponents of continental drift have amassed impressive geologic evidence to support their views. Indications of widespread glaciation from 380 to 250 million years ago are evident in Antarctica, southern South America, southern Africa, India, and Australia. If these continents were once united around the south polar region, this glaciation would become explicable as a unified sequence of events in time and space. Also, fitting the Americas with the continents across the Atlantic brings together similar kinds of rocks, fossils, and geologic structures. A belt of ancient rocks along the Brazilian coast, for example, matches one in West Africa. Moreover, the earliest marine deposits along the Atlantic coastlines of either South America or Africa are Jurassic (Jurassic Period) in age (approximately 200 to 145 million years old), which suggests that the ocean did not exist before that time.

      Interest in continental drift increased in the 1950s as knowledge of Earth's geomagnetic field during the geologic past developed from the studies of the British geophysicists Stanley K. Runcorn (Runcorn, Stanley Keith), Patrick M.S. Blackett (Blackett, Patrick M.S., Baron Blackett of Chelsea), and others. Ferromagnetic minerals such as magnetite acquire a permanent magnetization when they crystallize as constituents of igneous rock. The direction of their magnetization is the same as the direction of Earth's magnetic field at the time and place of crystallization. Particles of magnetized minerals released from their parent igneous rocks by weathering may later realign themselves with the existing magnetic field at the time these particles are incorporated into sedimentary (sedimentary rock) deposits. Studies by Runcorn of the remanent magnetism in suitable rocks of different ages from Europe produced a “polar wandering curve” indicating that the magnetic poles were in different places at different times. This could be explained either by the migration of the magnetic pole itself (that is, polar wandering) or by the migration of Europe relative to a fixed pole (that is, continental drift).

      However, further work showed that the polar wandering curves are different for the various continents. The possibility that they might reflect true wander of the poles was discarded, because it implies separate wanderings of many magnetic poles over the same period. However, these different paths are reconciled by joining the continents in the manner proposed by Wegener. The curves for Europe and North America, for example, are reconciled by the assumption that the latter has drifted about 30° westward relative to Europe since the Triassic Period.

      Increased knowledge about the configuration of the ocean floor and the subsequent formulation of the concepts of seafloor spreading (seafloor spreading hypothesis) and plate tectonics provided further support for continental drift. During the early 1960s, the American geophysicist Harry H. Hess proposed that new oceanic crust (ocean) is continually generated by igneous (igneous rock) activity at the crests of oceanic ridges (ocean)—submarine mountains that follow a sinuous course of about 65,000 km (40,000 miles) along the bottom of the major ocean basins. Molten rock material from Earth's mantle rises upward to the crests, cools, and is later pushed aside by new intrusions. The ocean floor is thus pushed at right angles and in opposite directions away from the crests.

      By the late 1960s, several American investigators, among them Jack E. Oliver and Bryan L. Isacks, had integrated this notion of seafloor spreading (seafloor spreading hypothesis) with that of drifting continents and formulated the basis of plate tectonic theory. According to the latter hypothesis, Earth's surface, or lithosphere (Earth), is composed of a number of large, rigid plates that float on a soft (presumably partially molten) layer of the mantle known as the asthenosphere. Oceanic ridges occur along some of the plate margins. Where this is the case, the lithospheric plates separate, and the upwelling mantle material forms new ocean floor along the trailing edges. As the plates move away from the flanks of the ridges, they carry the continents with them.

      On the basis of all these factors, it may be assumed that the Americas were joined with Europe and Africa until approximately 190 million years ago, when a rift split them apart along what is now the crest of the Mid-Atlantic Ridge. Subsequent plate movements averaging about 2 cm (0.8 inch) per year have taken the continents to their present position. It seems likely, though it is still unproven, that this breakup of a single landmass and the drifting of its fragments is merely the latest in a series of similar occurrences throughout geologic time.

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