9.1: The Earth's Interior
- Page ID
- 21743
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\(\newcommand{\avec}{\mathbf a}\) \(\newcommand{\bvec}{\mathbf b}\) \(\newcommand{\cvec}{\mathbf c}\) \(\newcommand{\dvec}{\mathbf d}\) \(\newcommand{\dtil}{\widetilde{\mathbf d}}\) \(\newcommand{\evec}{\mathbf e}\) \(\newcommand{\fvec}{\mathbf f}\) \(\newcommand{\nvec}{\mathbf n}\) \(\newcommand{\pvec}{\mathbf p}\) \(\newcommand{\qvec}{\mathbf q}\) \(\newcommand{\svec}{\mathbf s}\) \(\newcommand{\tvec}{\mathbf t}\) \(\newcommand{\uvec}{\mathbf u}\) \(\newcommand{\vvec}{\mathbf v}\) \(\newcommand{\wvec}{\mathbf w}\) \(\newcommand{\xvec}{\mathbf x}\) \(\newcommand{\yvec}{\mathbf y}\) \(\newcommand{\zvec}{\mathbf z}\) \(\newcommand{\rvec}{\mathbf r}\) \(\newcommand{\mvec}{\mathbf m}\) \(\newcommand{\zerovec}{\mathbf 0}\) \(\newcommand{\onevec}{\mathbf 1}\) \(\newcommand{\real}{\mathbb R}\) \(\newcommand{\twovec}[2]{\left[\begin{array}{r}#1 \\ #2 \end{array}\right]}\) \(\newcommand{\ctwovec}[2]{\left[\begin{array}{c}#1 \\ #2 \end{array}\right]}\) \(\newcommand{\threevec}[3]{\left[\begin{array}{r}#1 \\ #2 \\ #3 \end{array}\right]}\) \(\newcommand{\cthreevec}[3]{\left[\begin{array}{c}#1 \\ #2 \\ #3 \end{array}\right]}\) \(\newcommand{\fourvec}[4]{\left[\begin{array}{r}#1 \\ #2 \\ #3 \\ #4 \end{array}\right]}\) \(\newcommand{\cfourvec}[4]{\left[\begin{array}{c}#1 \\ #2 \\ #3 \\ #4 \end{array}\right]}\) \(\newcommand{\fivevec}[5]{\left[\begin{array}{r}#1 \\ #2 \\ #3 \\ #4 \\ #5 \\ \end{array}\right]}\) \(\newcommand{\cfivevec}[5]{\left[\begin{array}{c}#1 \\ #2 \\ #3 \\ #4 \\ #5 \\ \end{array}\right]}\) \(\newcommand{\mattwo}[4]{\left[\begin{array}{rr}#1 \amp #2 \\ #3 \amp #4 \\ \end{array}\right]}\) \(\newcommand{\laspan}[1]{\text{Span}\{#1\}}\) \(\newcommand{\bcal}{\cal B}\) \(\newcommand{\ccal}{\cal C}\) \(\newcommand{\scal}{\cal S}\) \(\newcommand{\wcal}{\cal W}\) \(\newcommand{\ecal}{\cal E}\) \(\newcommand{\coords}[2]{\left\{#1\right\}_{#2}}\) \(\newcommand{\gray}[1]{\color{gray}{#1}}\) \(\newcommand{\lgray}[1]{\color{lightgray}{#1}}\) \(\newcommand{\rank}{\operatorname{rank}}\) \(\newcommand{\row}{\text{Row}}\) \(\newcommand{\col}{\text{Col}}\) \(\renewcommand{\row}{\text{Row}}\) \(\newcommand{\nul}{\text{Nul}}\) \(\newcommand{\var}{\text{Var}}\) \(\newcommand{\corr}{\text{corr}}\) \(\newcommand{\len}[1]{\left|#1\right|}\) \(\newcommand{\bbar}{\overline{\bvec}}\) \(\newcommand{\bhat}{\widehat{\bvec}}\) \(\newcommand{\bperp}{\bvec^\perp}\) \(\newcommand{\xhat}{\widehat{\xvec}}\) \(\newcommand{\vhat}{\widehat{\vvec}}\) \(\newcommand{\uhat}{\widehat{\uvec}}\) \(\newcommand{\what}{\widehat{\wvec}}\) \(\newcommand{\Sighat}{\widehat{\Sigma}}\) \(\newcommand{\lt}{<}\) \(\newcommand{\gt}{>}\) \(\newcommand{\amp}{&}\) \(\definecolor{fillinmathshade}{gray}{0.9}\)The deep interior of the Earth remains somewhat of a mystery as we have only penetrated the very outermost 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. Geoscientists 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
Seismic activity gives us clues about 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.
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.
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 produce Earth's magnetic field.