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14.1: The Earth's Interior

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    The deep interior of the Earth remains somewhat of a mystery as we have only penetrated the very most outer portion with our deep drilling exploration. What knowledge we do have comes from seismic wave data or lava that has extruded onto the surface. What we do know is that the Earth's interior is somewhat like a concentric series of rings, progressing from the dense and intensely hot inner core toward the brittle outer shell of the crust. Geoscientist describe the layered interior of the earth on the basis of chemical composition or mechanical (physical) properties, like its ability to flow.

    Investigating the Earth's interior

    Figure \(\PageIndex{1}\): Seismograph recording seismic activity. (Courtesy USGS Hawaii Volcano Observatory)

    Seismic activity gives us clues as to the internal structure of the Earth. Geoscientists obtain seismic data from naturally occurring earthquakes or human-induced explosions. Seismic energy produces two kinds of waves that are useful in studying the Earth's interior. Compressional (P) waves generate a back-and-forth motion parallel to the direction of travel. Shear (S) waves move up-and-down perpendicular to the direction of wave transmission. Seismometers detect these motions and record them on a seismograph.

    When seismic waves pass through rock, their amplitude and direction changes. For instance, wave velocity generally increases as rock density increases. Shear waves do not penetrate molten masses and when they encounter a boundary between two rock types of differing densities, a portion of the wave travels along the boundary while another part returns to the surface. Such changes in seismic wave velocities led Yugoslavian geophysicist Andrija Mohorovicic (1857-1936) to discover the boundary between the crust and underlying mantle. Wave velocity increases through the "Moho" discontinuity. It is believed that the discontinuity represents a zone where sima-type minerals undergo a phase change that produces a new and denser combination of minerals. "Examine P and S waves moving through Earth's interior." (Courtesy NSF/TERC/ McDougall Littell)

    Video: The Solid Earth. Watch Professor Paul Tackley (Dept. of Earth and Space Sciences, UCLA) describe how the solid interior of the earth affects the outer layer through mountain ranges, volcanoes and plate tectonics. (Courtesy of

    Layers based on composition

    The outer brittle shell of the Earth is the crust that forms the "skin" of the lithosphere. The crust is primarily composed of silicate rocks and ranging in thickness of about 5 to 70 km (about 3 to 43.5 mi) The crust is broken into several continental and oceanic tectonic (lithospheric) plates. These plates ride atop the more pliable mantle beneath, colliding to create great mountain systems and spreading apart to form rift valleys.

    Figure \(\PageIndex{2}\): Interior Structure of the Earth (Click image to enlarge)

    The crust is divided into a basal zone of oceanic crust called the sima layer, and a less dense continental crust known as the sial layer. The sima is primarily composed of a heavy, dark group of basaltic rocks. Primarily composed of silica and magnesium, their high density (2800 to 3300 kg/m3) is due to the large amounts of iron and magnesium. The sial, named for the two predominate elements silicon and aluminum, is lighter in weight with densities around 2700 - 2800 kg/m3. Often geoscientists refer to rocks of the sial as "granitic rock" as granite is a predominant rock type. The lower boundary of the sial grades into the upper portion of sima. The sial actually has quite a diversity of rock types, including large amounts of basaltic rocks. The sima however is almost exclusively basaltic in composition. Separating the upper mantle from the oceanic crust is the Moho Discontinuity. Seismic waves passing though this boundary increase their wave velocity from 7 km (4 mi) per second to 8 km (5 mi) per second. The shift of wave velocity is due to the change in rock composition and density. The mantle is over 2900 km thick (1801 mi)and comprises 80% of the Earth's total volume. It is mainly composed of a dark, dense ultramafic rock called peridotite camera icon that is rich in iron and magnesium. Seismic wave velocity increases steadily through this zone. The core is composed of iron and nickel with a liquid outer region and a solid core. The core is about half the diameter of the Earth.

    Layers based on physical properties

    The lithosphere is a rigid cool layer composed of the crust and the uppermost mantle. The asthenosphere is the least rigid portion of the mantle. It is a soft, easily deformed layer that is susceptible to slow convection caused by pockets of increased heat from the decay of radioactive elements. The mesosphere (not to be confused with the atmospheric layer of the same name) lies between the asthenosphere and core where the pressures are so great the mantle is solid. Finally, the core with its molten outer and rigid inner layers. Though intense heat is generated at such great depths, geoscientists believe that under the enormous overlying pressure the inner core is made of solid iron and nickel. The outer core is thought to be molten iron because shear-wave velocities drop to zero which occurs when they encounter a liquid. The interaction between the inner and outer core is thought to produce Earth's magnetic field.

    Video: Difference between the crust and lithosphere (Courtesy Kahn Academy)

    This page titled 14.1: The Earth's Interior is shared under a CC BY-SA 4.0 license and was authored, remixed, and/or curated by Michael E. Ritter (The Physical Environment) via source content that was edited to the style and standards of the LibreTexts platform.