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Chapter 3 - Structure of the Earth

This chapter reviews the major concepts of the structure of the Earth and describes the dynamic processes associated the formation of distinct layers within the earth. This is essentail information to understand plate tectonics (discussed in Chapter 4). Plate Tectonics Theory is a fundamental theory that captures the science of how the earth works: why "things" are where they are, how they formed, and how they evolved, over time, to become features within the world that we see today.

While much has been discovered about the character and natural resources of our planet since the time of Christopher Columbus's first voyage, little was know about the internal character of the Earth until the Cold War era following World War II. Although studies of the internal structure of the earth were first reported in the late 19th century using seismic wave data from great earthquakes, it was the data from testing, spying, and verification of underground nuclear explosions that provided a clearer, more detailed picture of the internal structure of our planet. The earth is composed of several zones, including a central core, a mantle, and a crust (Figure 3-4 and 3-5). Oceans (hydrosphere) and atmosphere rest on the surface of the crust. All parts are held together and have their character based on the force of gravity, their chemical composition, and largely how they formed and changed through geologic time. These same factors apply to other planets and moons as well.The solid earth has a central core (both solid & liquid), a mantle, and the crust.

The appearance of the world as we see it today is a result of the accumulative effects of all geologic processes that have happened in the past. Some of these processes occur rapidly (such as volcanic eruptions, earthquakes, great storms and flood, and occasional asteroid impacts). However, most features we see on the landscape or in a region (or larger features like continents mapable on a global scale) involve processes that are far grander, operating both near and deep below the surface, and taking place gradually over long periods of time (in periods measured in millions to hundreds-of-millions of years). For instance, the coast lines of northwest Africa and the eastern United States are currently moving apart at a rate of about 2-4 inches a year. However, about 200 million years ago the two continents were joined together before the opening and formation of the Atlantic Ocean basin! Plate tectonics theory helps explain most of the processes and grand landscape features we observe around the world today, both on land and beneath the oceans.

Click on small images for a larger view throughout this website.
Volcanic eruption
Fig. 3-1. Nearly all geologic processes observed on Earth "fit" in in some way into "Plate Tectonics Theory."
Plate tectonics model showing types of plate boundaries
Fig. 3-2. A simplified model of plate tectonics showing types of lithospheric plate boundaries.

The Atmosphere

The atmosphere is gaseous mass or envelope surrounding the Earth, and retained by the Earth's gravitational field. The Earth's atmosphere is subdivided into levels:
* The troposphere is the lowest portion (up to about 6-8 miles) where all weather takes place and contains about 80% of the air's mass and 99% of water vapor.
* The overlying stratosphere contains an abundance of ozone which absorbs ultraviolet radiation, protecting life on land and in the shallow ocean extends up to about 31 miles.
*The mesosphere is the part of the earth's upper atmosphere above the stratosphere in which temperature decreases with altitude to the atmosphere's absolute minimum.
* The thermosphere the region of the atmosphere above the mesosphere and below the height at which the atmosphere ceases to have the properties of a continuous medium (about 60 miles). The thermosphere is characterized throughout by an increase in temperature with height. where the charged atomic particles of the solar wind begins to interact with atmospheric gases.

Layers of the atmosphere
Fig. 3-3. Structure of the Earth's atmosphere.

What is solar wind?

The solar wind is a stream of energized, charged particles (mostly electrons and protons), flowing outward from the Sun’ surface. The solar wind moves through solar system at speeds roughly 500 miles per second (800 km/sec; about 10 days from Sun to Earth) and can reach temperatures of about 1 million degrees (Celsius). The solar wind is what blows a "tail" away from the bodies of comets as they go through the solar system. Estimates suggest the Sun loses the equivalent of “one Earth mass” about every 150 million years (which isn't much considering the size of the Sun). Intense “corona ejections” from the Sun’s surface result in “solar storms” that frequently impact Earth and other planets. The Earth’s magnetic field shields the planet from the erosive effects of the solar wind. Particles trapped by Earth’s magnetic field flow into the upper atmosphere producing the Aurora Borealis (“Northern Lights”) and Aurora Australis (‘Southern Lights”). Over geologic time, the solar wind erodes the atmosphere of planets with weak magnetic fields (this includes Mars and the Moon).

Hydrosphere and Cryosphere

The hydrosphere includes all the waters on the Earth's surface, such as oceans, lakes, rivers, streams, and groundwater. 97% of all water on earth is seawater (discussed in Chapter 7).

The cryosphere is the frozen water part of the earth system including glaciers, sea ice, snow, freshwater ice, and frozen ground (permafrost).

The hydrologic cycle illustrates the movement of water through the hydrosphere and cryosphere. The movement of water and ice erodes the land surface and provide ocean basins with sediment. Dissolved materials become the salt in seawater. Salts in seawater are concentrated as water evaporates and later falls as precipitation, with most of it falling back into the ocean. The rest falls on land and becomes ice, runoff, groundwater, or is absorbed and released by living things, mostly plants.

The Water Cycle illustrated
Fig. 3-3. The hydrologic cycle illustrates the movement of water through the hydrosphere and cryosphere.

The Biosphere?

The term "biosphere" is the indistinctly defined regions of the surface, subsurface, and atmosphere of the Earth (or possibly other planets) occupied by living organisms. What we do know is that all life requires water. So far, a biosphere is only known to exist of Earth.

Subdivisions of the Structure of the "Solid" Earth

The Earth consist of several parts: a core, a mantle, and a crust. Other planets and moons in our Solar System share some of these characteristics:

* The crust is the outermost solid shell of a rocky planet or moon, which is chemically distinct from the underlying mantle. The crust is composed of light silicates rich in aluminum. The crust is a comparatively thin outer skin that ranges from 3 km at the oceanic ridges to 70 km in some mountain belts. Gravity measurements show that the crust is separated into thin oceanic (3.0 gm/cc) and thicker continental crust (2.7 gm/cc)

* The mantle is an inner layer of a terrestrial planet or other rocky body large enough to have differentiated in composition by density. On Earth, the mantle is a highly viscous layer between the crust and the outer core.
• Composed of heavier silicates rich in iron and magnesium that extends to a depth of about 2900 km.
• Large portions can flow slowly and are near melting.
* The core is the innermost part of the earth is believed to be an magnetic iron-nickel rich sphere that consist of a 758 mile thick solid and very dense inner core that is overlain by a 1400 mile thick zone of dense molten material in the outer core. Outer core is liquid, and heat convection here sets up Earth’s magnetic field. The metallic core is overlain by a rocky mantle.

Other "rocky" planets and moons have also cores, mantles, and crusts, hydrospheres, and atmospheres.
Structure of the earth showing the asthenosphere
Fig 3-4. The asthenosphere is a more "fluid" or "plastic" like part of the upper mantle immediately below the lithosphere (the cooler, more rigid uppermost part of the mantle and overlying crust).
 

Layers of the Earth as defined by physical properties

With increasing depth, Earth’s interior is characterized by gradual increases in temperature, pressure, and density.
Depending on the temperature and depth, a particular Earth material may behave like a brittle solid, deform in a plastic–like manner, or melt and become liquid.

Lithosphere (sphere of rock)

The term lithosphere is used to describe the rigid outer part of the earth, consisting of the crust and upper mantle. Compared with other layers of the Earth, the lithosphere is a relatively cool, rigid shell and averages about 100 km in thickness, but may be 250 km or more thick beneath the older portions of the continents. Processes occurring in Earth's lithosphere are responsible for all the large-scale features observable on the surface (including ocean basins, continents, and mountain ranges).

Asthenosphere (weak sphere)

The term asthenosphere refers to a semi-fluid layer beneath the lithosphere (within the upper mantle), between about 40 to 80 miles (100-600 km) below the outer rigid lithosphere (oceanic and continental crust) forming part of the mantle. The asthenosphere behaves "plastically" and can mechanically detach from the lithosphere.and is thought to be able to flow vertically and horizontally, enabling sections of lithosphere to subside, rise, and undergo lateral movement associated with plate tectonics. The asthenosphere can move independently of the lithosphere.

Mesosphere (or lower mantle)

This region is a rigid layer between the depths of 660 km and 2900 km, but the rocks at these depths are very hot and capable of very gradual flow. Heat from the core drives gradual mantle convection.

Outer core:
As discussed above, the outer core is a liquid layer composed mostly of an iron-nickel alloy (similar to metallic meteorites). Convective flow within the outer core generates Earth’s magnetic field.

Inner core: Geophysical studies show that the inner core behaves like a solid, but is very dense, around 16 gm/cc (like an iron-nickel meteorite)

Structure of the Earth
Fig. 3-5. Structure of the Earth
Iron-nickel meteorite
Fig. 3-6. An iron-nickel meteorite is magnetic and has a similar density as the metallic core of our planet.
 
How do we know the structure of the Earth? By indirect geophysical methods! Geophysical methods use technical applications and equipment to collect information about the earth, oceans, and atmosphere that are not directly observable by our senses. Examples include:

Geophysical Method
Instruments Used
Magnetic measurements
magnetometers
Gravity measurements from the surface or from precise measurements from satellites orbiting a planet or moon
gravitometers and satellites
Seismic waves from earthquakes or large explosions
seismographs
International Space Station
Fig. 3-7. Gravity can be precisely measured from orbiting satellites.

Magnetism measurements reveals the Earth's metallic core

Earth's magnetic field is believed to be associated with the Earth's inner metallic core and possibly hot molten metallic material of the outer core. Measurements of Earth's magnetic field support evidence that it forms from convection in the liquid metallic outer core. There must be significant amounts of iron for Earth to have such a strong magnetic field.

The magnetic compass was invented in China and has been in use since the 2nd century BC. The Geographic North Pole is currently offset from the Magnetic North Pole by about 11.5 degrees (same with the South Poles). The magnetic poles are very slowly wandering, showing that their magnetic orientation is linked to the Earth's metallic core, not the mantle or lithosphere.

Magnetic Reversals: The N-S dipole part of the Earth’s magnetic field reverses, causing the locations of the north and south magnetic poles to switch. Magnetic reversals have happened happened many times through geologic time. Magnetic reversals are preserved in the “paleomagnetic record” - preserved as weak magnetic fields locked into rocks bearing magnetic minerals at the time they form (see Paleomagnetism discussion below). Current thought is that the magnetic reversals are caused by shifting currents in the liquid metallic outer core.
Earth's magnetic field
Fig. 3-8. Earth's magnetic field extends from the core and far out into space.
 

Gravity Measurements

Gravity measurements reveal that there must be denser material deeper in the earth. Rocks at the surface of the planet are not dense enough to account for the overall higher amount of gravitational attraction that exists between objects on the surface and objects orbiting the planet. Variations in gravitational forces also reveal subtle differences in the density and thickness of the crust in different regions of the world.

Newton's Law of Universal Gravitational Attraction
Gravitational Attraction = g * (m1 * m2)/r*r
g = the gravitational constant
m1 = mass of the first body
m2 = mass of the second body
r = radius between the two bodies
Gravity measurements can be made anywhere on the surface using gravitometers (devices that measure very tiny differences in Earth's gravitational field from one place to another). Gravity measurements are also calculated measuring subtle changes in the paths of Earth orbiting satellites.



Gravity Anomaly Map
Fig. 3-9. NASA's gravity anomaly map shows subtle differences in the Earth's gravitational field in different portions of the world.
 

Seismic Waves

Seismology is the study of earthquake shock waves as they pass through the earth. Seismology is the science that helped resolve many questions about the internal structure of the earth.

Seismic waves are shock wave and vibrations in the Earth which issue from the focus of an earthquake. Seismic waves are a result of an earthquake, impact, or explosion, or some other process that imparts low-frequency acoustic energy into the earth. (Figures 3-10 and 3-11).

Two types of seismic waves
: surface waves and body waves
surface waves travel on the surface
body waves travel through the earth. There are two types of body waves: P waves and S waves

P (primary) waves are compressional and move parallel to wave movement.
• P waves travel through denser and more compact elastic materials (solid, liquids, gases) faster than S waves.

S (shear) waves have a shear effect and move perpendicular to the waves movement.
• S waves do not travel through liquids or gas and are slower than P waves.
Terms used to describe earthquakes

earthquake—ground shaking caused by a sudden movement on a fault or by volcanic disturbance.

fault—
A fracture or crack along which two blocks of rock slide past one another. This movement may occur rapidly, in the form of an earthquake, or slowly, in the form of creep. Types of faults include strike-slip fault, normal fault, reverse fault, and thrust fault.

epicenter
—The point on the Earth’s surface above the point at depth in the Earth’s crust where an earthquake begins.

focus
—the point below the Earth's surface where seismic waves originate during an earthquake.


Earthquakes occur somewhere around the world every hour of every day. Most are too small to even feel—however, large-magnitude, damaging earthquakes happen somewhere around the world almost every year. Large earthquakes in unprepared regions can cause widespread chaos, destruction, and death. Earthquakes are associated with faults, but not all faults currently generate earthquakes (they may have been active long ago). Faults range is size from small fractures in a local outcrop to great fault systems that can extend for thousands of miles. Below are key terms used to describe earthquake phenomena.

rupture zone—the area of the Earth through which fault movement occurred during an earthquake. For large earthquakes, the section of the fault that ruptured may be several hundred miles in length. Ruptures may or may not extend to the ground surface.

A seismograph is a device used to record earthquake shaking and are used to determine the distance, magnitude and intensity of earthquakes. Data from numerous seismographs linked together in networks are used to determine the focus, epicenter, extent of rupture, and amount of shaking in a region caused by an earthquake. A minimum of 3 seismographs are needed to determine the epicenter of an earthquake (Figure 3-12).

Note that the Global Seismographic Network consists of hundreds of seismographs around the world, so information about earthquakes can be calculated quite precisely.

earthquake magnitude (M)
—A numeric measure that represents the size or strength of an earthquake, as determined from seismographic observations. The Richter scale is a numerical (logarithmic) scale for expressing the magnitude of an earthquake on the basis of seismograph oscillations. Today earthquake intensity is recorded with a moment magnitude scale (MMS) which is based on the seismic moment of the earthquake, which is equal to the rigidity of the Earth multiplied by the average amount of slip on the fault and the size of the area that slipped. Richter scale and moment magnitude scales are similar, but the MMS scale is more precise (Figure 3-13).

earthquake intensity (I)—
A measure of ground shaking describing the local severity of an earthquake in terms of its effects on the Earth’s surface and on humans and their structures. The Modified Mercalli Intensity (MMI) scale, which uses Roman numerals, is one way scientists measure intensity (Figure 3-13).

Video: Historic Earthquakes compared (Pacific Tsunami Warning Center)

Focus and epicenter of an earthquake
Fig. 3-10. Diagram illustrating the epicenter and focus of an earthquake along a fault.
Earthquake S waves and P waves
Fig. 3-11. Earthquake waves include:
P-compression wave and
S-shear wave
P-waves move faster than S-waves and are first to be felt, the S-waves arrive next and produce the majority of shaking in an earthquake.
Three seismographs locating the epicenter of an earthquake
Fig. 3-12. At least three seismographs are needed to locate the epicenter of an earthquake. A single seismograph can only tell you how far away an earthquake occurred, but not in which direction.
Comparison of Magnitude and Intensity scales
Fig. 3-13. Comparison of earthquake magnitude (MMS) and intensity (MMI)scales (USGS)
 

How do seismic wave data revealed the internal structure of the Earth?

Earth's Shadow Zones: Extensive study of shock waves of earthquakes and the global monitoring of underground nuclear bomb testing revealed information about the internal structure of the Earth. P and S waves both go through solids. S waves do not go through non-solids, so only P waves are received on the opposite side of the earth. No P or S waves are received on the sides, but for a different reason. Zones of "seismic wave shadows" in the regions between about 105° to 140° on the opposite side of the globe from a seismic shock source revealed that part of the Earth's core is liquid material (molten material)(Figure 3-14). In contrast, an inner core is believed to consist of solid metal, possibly similar in composition of iron meteorites.

What can seismic (P and S) waves data tell us?

• Parts of the earth are not solid.
• The depth and location of an earthquake (EQ).
• The relative strength of an EQ.
• The average density of earth.
• The density of each layer in the earth.

Seismic waves passing through the earth reveal earth's structure
Fig. 3-14. Seismic shock wave provide information about the structure of the Earth.

Earth’s major boundaries revealed by seismic waves

The "Moho" (Mohorovicic discontinuity): (Discovered in 1909 by Andriaja Mohorovicic)
• Separates less dense crustal materials from underlying mantle
• Identified by a change in the velocity of P waves

The core-mantle boundary (CMB): (Discovered in 1914 by Beno Gutenberg)
• Based on the P-wave shadow zone
• No P waves from 105 to 140 degrees
• The fact that S waves do not travel through the outer core provides evidence for the existence of a non-solid layer beneath the mantle
• Showed existence of liquid outer core and overlying mantle

Lehmann Discontinuity (Predicted by Inge Lehmann in 1936)
• Boundary between outer and inner core defined by an increase in seismic wave velocity from outer to inner core and by seismic wave reflection off the solid inner core.

Structure of the Earth
Fig. 3-15. Structure of the Earth diagram shows the locations of the Moho, CMB, and Lehmann Discontinuity.
 

Seismic wave data used to map the lithosphere

Earthquake data also reveals the location of major fault zones of the world (Figure 3-16). Many of the fault systems are associated with lithospheric plate boundaries (see discussion below).

Fault systems evolve and change over time
—driven by plate tectonic forces associated mantle convection influencing the rigid lithosphere. Fault systems are often associated with volcanic regions. Faults may form and remain active for long ages before becoming inactive, and then may become reactivated again in some later period. Tectonic forces within the Earth deform rocks through processes of folding and faulting, producing many of the landscape features observable around us.
Earthquake map of the world
Fig. 3-16. Map of earthquakes of the world (USGS record for 1978 to 1987).

Mantle Convection

Heat convection in the mantle is the source of forces that move, bend, and break rocks in the Earth's lithosphere (Figure 3-17). Heat in the earth is mostly left over from when the Earth formed billions of years ago in the solar system's nebula. Heat is also generated by the decay of radioactive elements and possibly gravitational tidal forces.

Motion within the mantle is responsible for deep crustal stretching (extension) and compression. Motion in the mantle is produced by heat convection—hot rocks expand and rise whereas cooler (hence denser) rocks sink. Thicker, less dense, continental crust floats higher than thinner, denser ocean crust below ocean basins.

Deformation is the action or process of changing in shape or distorting, especially through the application of pressure. In geologic terms, deformation refers to changes in the Earth's crust related to tectonic activity, particularly folding and faulting.

Heat from inside the earth drives mantle convection (hot material rises, cool material sinks, Figures 3-17). The rise and fall of masses of material in the material in the mantle create forces that move the rocks in the cool and brittle lithosphere near the Earth's surface. These motions exert great forces, strong enough to rip continents apart, but the rate of movement is extremely slow on an annual basis (measurable in inches or centimeters).

Whereas the "fluid-like" state of rocks in the asthenosphere move slowly, the solid, brittle material in the lithosphere builds up great pressure (stresses) and the rocks will strain under the pressure until the point that they rupture, causing an earthquake that propagates as a shockwave through the earth.
Mantle convection
Fig. 3-17. Mantle convection is the driving force of movement in the Earth's lithosphere. Gravity-driven heat convection within the Earth is the conclusive power source driving plate tectonic motions.
 

Behavior of the Lithosphere (rigid crust and upper mantle) and Asthenosphere (upper mantle)

Subdivisions used in geologic discussions relating to "Plate Tectonics Theory" (discussed below) include:

The Lithosphere is the rocky outer portion of the Earth, consist of the crust and upper mantle (about the upper 60 miles below the Earth's surface). It is the solid "brittle" zone of the earth where earthquakes occur.

The asthenosphere
is the upper portion of the mantle underlying the lithosphere where heat and pressure is great enough for materials to flow "like plastic." This movement is driven by the heat derived from within the deeper parts of the mantle and core that cause materials to flow by gravitational heat convection (see Figure 3-17). Gravitational convection works as follows—Adding heat causes materials (solid and molten) to expand, loose density, and rise; whereas cooling material shrinks and increases in density, and sinks. The asthenosphere is a semi fluid layer of the earth, between about 40 to 80 miles (100-200 km) below the outer rigid lithosphere (oceanic and continental crust) forming part of the mantle and thought to be able to slowly flow vertically and horizontally, enabling sections of lithosphere to subside, rise, and undergo lateral movement associated with plate tectonics.

Another important distinction within the lithosphere are the differences between what is known as "oceanic crust" and "continental crust." The rocks exposed on continental land masses are different than those found beneath the ocean basins.

ocean crust—part of Earth's lithosphere that underlies ocean basins. Oceanic crust is primarily composed of mafic rocks (rocks rich in iron and magnesium) and are less dense than rocks that underlie continents (continental crust rocks are enriched in silica and aluminum). Ocean crust around the world is significantly younger (less than 200 million years) relative to continental crust which has typically accumulated through the natural refining processes associated with plate-tectonics over many hundreds of millions to several billion years.

continental crust—the relatively thick part of the earth's crust that forms the large landmasses. It is generally older and more complex than the oceanic crust, and dominantly composed of igneous and metamorphic of granitic or more felsic composition (rocks are enriched in silica and aluminum).

In general, rocks found within continental landmasses "collectively" are less dense than rocks recovered from beneath the ocean basins. This difference helps explain the geography of the planet as well as explaining many aspects of the tectonic forces changing the landscapes of our planet over time.

Isostacy illustrated
Fig. 3-18. Isostacy: floating wooden blocks of different sizes illustrate how oceanic and continental crustal rocks are at relative isostatic equilibrium floating on the mantle. There would have to be more "light" crust under mountain ranges than under oceans. As geophysical studies reveal, continental crust is typically thicker and less dense than ocean crust.
Himalayas and Tibet
Fig. 3-19. Crustal thickening in the Himalayan Mountains and Tibetan Plateau is illustrated in this photograph from space.

Isostacy

Isostacy is the state of balance, or equilibrium, which sections of the earth's lithosphere (whether continental or oceanic crust) are thought ultimately to achieve when the vertical forces upon them remain unchanged. In the early days of "modern geology" the variations in elevations on land (topography) and the depth of the oceans (bathymetry) were mapped around the globe. Investigations lead to the hypothesis of isostacy, that continents were floating on a more fluid mantle, much the way that wood blocks or icebergs float on water. With wood or ice blocks, the thicker they were, the higher they rose above the water (Figure 3-18). This lead to the belief that the crust beneath the continents—especially beneath mountain ranges—is "thicker" and "less dense" than the crust beneath the ocean basins. To maintain an isostatic equilibrium there had to be an equivalent amount of "lighter" crustal material beneath a mountain range in order for it to rise to higher elevations. For example, the crust beneath the Himalayan Mountains must be much thicker that the crust beneath the Indian mainland, and much thicker than the crust beneath the Indian Ocean (Figure 3-19). Isostatic equilibrium is the state of balance which sections of the earth's lithosphere (whether continental or oceanic crust) are thought ultimately to achieve when the vertical forces upon them remain unchanged. The lithosphere floats upon the semi-fluid asthenosphere below (see Figure 3-18).

Geologic Examples of Isostacy

An iceberg floating on the ocean is a perfect illustration of isostacy (Figure 3-20). At Earth's ocean surface, solid freshwater glacier ice is about 10.7% less dense than cold seawater; as a result, ice floats. The amount of ice rising above the ocean surface is in equilibrium with the buoyant ice below the surface. As icebergs melt, the amount of ice above the surface adjusts to the buoyant volume below the surface. The ratio of the amount of ice above and below the surface remains the same as the ice melts.

Isostacy also causes deformation of rocks. For example, If a section of lithosphere is loaded, as by ice of a continental glacier, it will slowly subside to a new equilibrium position. When the continental glacier melts, the removal of the weight allows to slowly rebound back to isostatic equilibrium. Parts of northern North America and Europe that were covered by continental glaciers during the last ice age are now slowly rising eventually back to isostatic equilibrium (this action is called glacial rebound) (Figure 3-21).

The crust is always readjusting to changing forces from below and above. If a section of lithosphere is reduced in mass, as by erosion, it will slowly rise to a new equilibrium position. Increases in heat flow from the mantle cause crustal rocks to warm, expand, and rise. Old ocean crust becomes cold and shrinks, and with its mafic composition becomes denser and sinks back into the mantle.

An iceberg illustrates isostacy.
Fig. 3-20. Iceberg showing isostacy. Ice below the surface is in equilibrium with buoyant ice below the surface. As the ice melts, the iceberg floats lower and lower in the water.
Glacial rebound of continental crust floating on the asthenosphere
Fig-21. Isostatic rebound caused by the melting of continental glaciers reveals the "fluid-like" behavior of the asthenosphere.

Isostacy and the "Age of Landscapes"

Many hypotheses were put forward to try to explain the evolution of landscapes—isostacy was one of them. Early hypotheses focused on what was easily observable. Continents around the world shared a variety of large physiographic features: mountain ranges, coastal plains, plateau regions, and inland lowlands. Some of these lowland regions are underlain by what appeared to be ancient rocks that were once to core of mountain ranges in the distant past. These regions were located near the center of most of the continents and have became known as "shields" (such as the Canadian Shield of North America, see Figure 3-22). In most cases, these "shields" are surrounded by belts of mountain ranges that were composed of rocks that appeared younger than the shield regions. Also, some of these mountain ranges appeared much "younger" than other mountain ranges. This lead to conclusions that landscapes could be classified as "youthful," "mature," or "old age" - assuming that all mountain ranges form about the same way, and that "youthful" mountain ranges, like the Himalayan or Rocky Mountains eventual erode way (becoming more "mature" with age, like the Appalachian Mountains). Eventually almost all elevated features (mountains, hills) completely erode away, producing "old age" landscapes, similar to what is seen in shield regions (see Figure 3-22).

The assumption is that as materials erode away, the crust readjusts itself to maintain an isostatic equilibrium. As material is removed the crust rises. Over time, material that were once deep within mountain ranges eventually becomes exposed at the surface by erosion. Over time, the assumption was that isostatic adjustments eventually cease, and the mountains would completely erode away to a flat plain and eventually sink below the waves. Unfortunately, there were too many cases where the isostatic adjustment hypotheses didn't match all the observable facts. Not all old shield regions were low plains (as illustrated with the Scandinavian region of Europe and much of Africa). In addition, some regions, such as the Colorado Plateau, had characteristics that fit into all three categories, youthful, mature, and old age, all at the same time. In addition, there was very little to explain how mountain ranges and continents formed in the first place! Why do some mountain ranges have volcanoes and other don't? What would explain the composition and distribution of volcanic mountain ranges around the world, and what in the world could explain what chains of volcanoes like the Hawaiian archipelago were doing in the middle of the Pacific Ocean? These questions (and more) were finally resolved with the development of Plate Tectonic Theory.



Crustal isostacy over time compared with youthful, mature, and old age landscapes
Fig. 3-22. Isostacy and the hypothesis of landscapes evolving through "youthful," "mature" and "old age" stages. Evolution of a landscape over time involves uplift, erosion, and isostacy.
 

Plate Tectonics Theory

Plate Tectonics is a unifying collection of concepts that explains most things geological on Earth, and other planets and moons as well. (Note: Plate Tectonics is the focus of Chapter 4). Plate Tectonics theory explains the structure of the Earth's crust and many associated phenomena as resulting from the interaction of rigid lithospheric plates that move slowly over the underlying mantle. Heat convection in the mantle is the driving force that rigid lithospheric plates across the globe.

Plate Tectonics (definition)
• A theory that states that the earth's solid outer shell (lithosphere) broken into "plates" can move relative to each other while sitting over a plastic, non-solid layer called the asthenosphere.
• Convection in the asthenosphere is thought to be the driving force.
• The lithosphere/asthenosphere boundary is most important for this movement to occur.
• Most volcanic and seismic activity occurs where the solid lithospheric plates meet.
Plate Tectonics
Fig. 3-23. General model representing essential concepts presented by Plate Tectonics Theory (discussed in Chapter 4).

Historical Observations leading up to Plate Tectonics Theory

Much of the background work related to the modern theory is the culmination of hundreds of years of world-wide exploration and geologic observations in the 1600-1700-1800’s. Highlights include:

* Early Maps of the World: Maps compiled by early global explorations resulted in the observation of the similarities of coastline patterns on opposite sides of the Atlantic Ocean. These similarities were noted from early maps by by a Flemish cartographer named Abraham Ortelius in 1596 who first suggested that it looked like the continents had "drifted apart." Geographers preparing maps noted that charts of land masses that the shape continents of the world "fit" together like a jig-saw puzzle. It took centuries before an organized effort started to analyze the data!

* Observations of the location of the world's volcanoes (maps) and lead to the recognition of the "Ring of Fire" (Figure 3-24).

Continental Drift

The Continental Drift Hypothesis was an prelude to the modern Plate Tectonics Theory. Many of the observable facts from the early investigations of continental drift are fundamental to the newer theory.

The Continental Drift Hypothesis was proposed by a German astronomer and meteorologist named Alfred Wegener (1880-1930), but based on research by other earlier observers. The Continental Drift Hypothesis was based on observations that the continental coastlines on either side of the Atlantic Ocean seemed to match up and was also supported by paleontological and geological comparisons on the continents bordering the ocean.

From Alfred Wegener's Continental Drift Hypothesis came the "slow to be accepted" theory that all the observable continents bordering the Atlantic and Indian Oceans had once assembled into a single supercontinent he named "Pangaea," and that this great landmass began to break apart about 200 million years ago (Figures 3-25 to 3-27). He said that these continents started moving about 200 million years ago (MYA) and they are still moving. This is amazing because it is pretty accurate.

Pangaea—a supercontinent comprising all the continental crust of the earth, theorized to have assembled from other continental land masses in middle to late Paleozoic time. The assembled landmass, Pangaea, existed through late Paleozoic and through early Mesozoic times before the component continents separated and gradually migrated into their current configuration.

Geologic and fossil trends indicated that some land masses which are now separated may have been together at some point in time. However, nobody could provide a mechanism for the continents to move. Whereas the geologic and paleontological evidence (fossils) on continents on opposite sides of Atlantic Ocean basin and parts of the Indian Ocean basin provided fairly conclusive evidence supporting continental drift (Figures 3-26 and 3-27).

Fossil evidence supporting Continental Drift includes:
• Similar fossil sites occur on different continents, when "Pangaea" was together. Examples include Mesosaurus and Glossopteris fossils (Figure 3-26). Mesosaurus is a reptile from the Early Permian of southern Africa and South America. Glossopteris are fossilized woody plants from the Permian and Triassic Periods.
• Fossils and organic deposits in sedimentary rocks provide information about the geologic features, the climate, and flora and fauna for an area through geologic time.
• In many regions, fossils are found presently in climates and locations that could not have supported them. Example: fossil corals found in marine sediments of northern Alaska.
• Fossils show that marked "divergent evolution" occurred at times when the continents were split apart. This can account for the present-day distribution of plants and animals around the globe (especially marsupial mammals).

Geologic features supporting Continental Drift include:
Old mountain ranges cross continental boundaries that are now separate but were once together. (Examples: The Appalachian Mountains in eastern US and Atlas Mountain of northwest Africa).
• The formation of rocks in climates that could not support those types of rocks. Example: Permian-age rocks displaying evidence of glaciation in found in southern India.
The Sedimentary Rock Record in many regions around the world reveals the progression of changes that took place as continental landmasses split apart. For example, When Africa pulled apart from South America the sediments reveal:

• First, the land was uplifted, rifted apart, and a very large lake filled in the low region.
• The rift partially opened to the ocean from the north.
• Finally, it opened completely to the open ocean to the south.
• This occurred between 60 and 100 million years ago.


* Similar processes are occuring in the African Rift Zones and Red Sea region today!

The Atlantic-Pacific Paradox

Early exploration of Atlantic Ocean basin showed that it is surrounded mostly by gentle coastal planes and old, worn down mountain ranges, and by comparison to other regions had relatively little volcanic or earthquake activity. In contrast, the Pacific and other ocean regions were much less understood.In contrast, Early exploration of the Pacific Ocean basin brought awareness of the region described as the "Ring of Fire" (see Figure 3-24). In most places places around the Pacific Rim ("Ring of Fire") the transition zones of the continents to the deep ocean has large numbers of active or "recently" active volcanoes. This region also experiences large numbers of sometimes tremendous earthquakes. In most places where volcanic arcs (island belts and mountain ranges composed of volcanoes) appear on land, there are also very deep-water trenches located not too far offshore of the coastline.

Why was "Continental Drift" rejected by the Scientific Community?

Although Continental Drift intrigued the scientific community, it was largely rejected because there was no data to explain all the observable facts about how or why continental plates moved across ocean basin. This was largely because in the early 20th century very little was known about the nature of the world's ocean basins nor the physical characteristics of the structure of the Earth's asthenosphere and lithosphere. Many other hypotheses existed in the scientific community well into the late 20th century, but these conflicting ideas have faded in significance with the advances of the newer Plate Tectonics Theory. Wegener's hypothesis was rejected because he proposed a mechanism for continental drift, which turned out to be wrong.

• His mechanism was complicated and involved the force of the earth spinning and the tides.
• He was dismissed as a crank and his detractors said that he carefully picked his data to fit his hypothesis.
• At this point in time the entire earth was believed to be solid, so it was difficult to formulate a mechanism for continental drift.

Rig of Fire
Fig. 3-24. The "Ring of Fire" is a zone of volcanoes, numerous earthquakes, and offshore deep trenches.
Pangaea
Fig. 3-25. Geographers noted that the continents fit together like a jig-saw puzzle.
Pangaea fossils
Fig. 3-26. Fossil evidence connecting lands of Pangaea about 260 million years ago)
Plate Motion
Fig. 3-27. The formation and breakup of Pangaea over 300 million years.
 

Seafloor Discoveries in the 20th Century

Although using sound to measure the depth of water was invented early in the 19th century, advanced methods were not widely used to intentionally map the seafloor until WWI and used in association with ship and submarine warfare activities. SONAR (short for "SOund NAvigation & Ranging") is a system for detecting objects under water and for measuring the water's depth by emitting sound pulses and detecting or measuring their return after being reflected off the seafloor. Sonar investigation revealed the extent of the Mid-Atlantic Ridge in the center of the Atlantic Ocean basin (Figure 3-28).

Seismology
has revealed important aspects of how lithospheric plates interact with each other, how plates form and are destroyed. In the 1930’s a Japanese scientist, Kiyoo Wadati, thought that deep earthquakes and volcanoes in Japan (and the Pacific Rim) could be explained by continental drift motions. Over time, as earthquake detection equipment (seismographs) were set up around the world and data collections were compiled, it became apparent that there were patterns that showed that nearly all earthquakes occurred in zones where chains of volcanoes and mountain ranges were most actively forming around the Ring of Fire, across southern Europe into east Asia, and along narrow belts beneath the oceans associated with mid-ocean ridges (Figure 5-28). Hugo Benioff (a USGS earthquake scientist) expanded on Kiyoo Wadati's ideas and plotted the location of deep earthquakes to delineated large geologic structures associated with the "Pacific Ring of Fire". It was recognized that earthquakes and volcanoes did not occur at random but at specific and concentrated spots on and within the earth's crust.
Map of the Atlantic Basin
Fig. 3-28. Seafloor bathymetry of the Atlantic Basin (mapped with SONAR) showing the Mid-Atlantic Ridge, a submarine mountain chain in the middle of the Atlantic Ocean.
 

Paleomagnetism and the study of the seafloor

Earth's magnetic field has been a curiosity since ancient times. The magnetic compass was first invented as early as the Chinese Han Dynasty (about 206 BC). The compass was used during China’s Song Dynasty for military navigation by 1044 AD, and for maritime navigation by about 1117 AD. Today, the source of the magnetic field is presumed to be from the movement of molten iron and metals in the earth's core. The "spinning" of these liquid metals produces electric currents in the same manner as an electric coil produces a magnetic field. The magnetic field extends into space (see Figure 3-8). Over time, these currents fade, change direction, or intensify elsewhere, causing the magnetic poles to migrate or reverse the magnetic polarity of the entire planet (events called magnetic reversals).

Magnetometers (devices used to magnetic fields) were used in World War II to search for submarines. It was noted from these investigations that the seafloor preserved mapable magnetic anomalies that parallel the Mid Atlantic Ridge (Figure 3-28). These investigations showed that that the earth's magnetic field has reversed many times through earth history; magnetic reversals happened over periods ranging from thousands to millions of years.

Paleomagnetism
is the study of the fixed orientation of a rock's magnetic minerals as originally aligned at the time of the rock's formation. Paleomagnetism is usually the result of thermoremanent magnetization (magnetization that occurs in igneous rocks as they cool below the Curie Point). Igneous rocks may keep their magnetic orientation they obtain at the time they form (if they are not altered). This magnetic signature is preserved, even if the landmass the magnetic rocks are on is moving. Mapping of the seafloor with magnetometers revealed lines of rock preserving history of "magnetic reversals" running parallel to the mid-ocean ridges [first published by Vine & Matthews, 1963] (Figure 3-29 and 3-30).

Seafloor spreading is the processes associated with the formation of new areas of oceanic crust, which occurs through the upwelling of magma at mid-ocean ridges and its subsequent outward movement on either side. As new rock forms along spreading centers it becomes attached to the lithospheric plates on either side of the spreading centers.

Paleomagnetic studies of the world ocean basin resulted in the discovery of mid-ocean ridges and spreading centers. These undersea mountain ridges extend for 10s of thousands of miles beneath portions of the global ocean basins (see Figure 3-16 and 3-28). Seafloor spreading became a mechanism to explain "continental drift". However, seafloor spreading alone does not explain the formation of continental landmasses through geologic time.

Paleomagnetism (old magnetism)

As rocks (with iron in them) solidify, the magnetism direction points to the magnetic pole (currently north).
The magnetic polar reversals have happened many times in earth history, and their ages are well known
Good for rotational problems and inferring latitude as continents have moved across the globe over time.
Important data for resolving the age of rocks, where they formed, and where they have traveled over time
Fundamental information about the formation of new oceanic crust and explains the migration of landmasses over time.
Magnetic reversals
Fig. 3-29. Mapping of the seafloor with magnetometers revealed lines of "magnetic reversals" on opposite sides of mid-ocean ridges. (USGS)
Magnetic ridge, Juan de Fuca
Fig. 3-30. West Coast magnetic reversals reveal the location of spreading centers and fault boundaries in the ocean basin offshore of California, Oregon, Washington, and British Columbia

Another Geologic Paradox: the differing ages of rocks within continents and beneath ocean basins

an the Late 1940's methods of radiometric-age dating was developed. After WW2, samples of ocean crust as sediments were collected from the sea floor throughout the world ocean basins and analyzed using both radiometric-age dating (decay or radioactive isotopes) and relative dating (using "microfossils" derived from seafloor sediment coring samples). Geologic data indicated a relatively young sea floor (ocean crust), where the oldest is about 200 million years old. However, data also indicated very old continents, where the oldest was more than 3 billion years old!
  • Continental crust is made up of rocks measured into the billions of years, especially in the stable "craton" cores of continental shields (mostly in the central region of continental landmasses) (Figure 3-31).

  • The oldest ocean crust is about 200 million years (Figure 3-32) The oldest ocean crust is found in locations near continental land masses (such as the east coast of North America) and near volcanic island arcs along the western side of the Pacific Basin.
As shown in Figures 3-31, 3-32, and 3-33, the maps shows the bathymetry and geologic ages of the ocean basins, highlighting long undersea mountain ranges (mid-ocean ridges) that extend thousands of miles near the middle of the Atlantic and Indian Oceans, and part of the eastern Pacific Ocean basin. Although early oceanographic studies revealed mountains hidden beneath the oceans, a complete map of the ocean floor wasn't compiled in detail until starting in World War II as part of naval research for submarine warfare. Although some data regarding the age of continental rocks was partly known before the war, much detail of the geology of continental regions wasn't available until global energy and mineral resource mapping was conducted in the decades following the war.

What was discovered was that, in general, most of the oldest rocks found in the Earth's crust occur in the center of continental landmasses, such as in the Canadian Shield region of North America, Greenland, the central parts of Africa, South America, Australia, and Siberia, and the peninsula of India (Figure 3-31).Thee regions have rocks that range in age to typical over a billion years to the oldest know rocks of about 4.4 billion years (from Australia). These regions are called continental shields. Note that It is within these regions that most of the world's most economically significant gem and precious metal deposits are found!

Surrounding the continental shields on most of the continents are belts of mountain ranges and coastal plains that contain rocks younger that a billion years in age. The higher mountain ranges, including the Himalayan, Andes, Alps, and Rocky Mountains are considered to be actively forming and are dominated by rocks that have formed after the breakup of the supercontinent Pangaea (mostly after about 300 million years ago). There are some older mountain ranges, like the Appalachian Mountains in eastern North America, that appear more worn down, and the areas are relatively inactive geologically (having fewer earthquakes and little recent volcanic activity). By comparison, the landscapes within the shield regions are nearly completely worn down and are no longer "geologically active." However, these shield regions display characteristics of having once been parts of mountain ranges that existed a billion or more years ago. In many areas parts of the shield regions, ancient mountain ranges have formed, eroded away, and reformed again and again, but today, in contrast, there is very little geologic activity (volcanoes or earthquakes).

Figure 3-32 is a map showing the age of rocks found in the crust beneath the ocean basins of the world. Again, beginning in ernest during World War II and culminating in the Cold War, geophysical mapping and sampling of materials from the sea floors around the globe showed that rocks on the ocean basins were very significantly younger that rocks found on the continents, with ages ranging in only about 200 million for the oldest rocks beneath ocean basins! In all cases, the age of seafloor grows progressively younger approaching the mid-ocean ridges. Using seismic data and deep-sea submersible exploration craft, the mid-ocean ridges were discovered to be belts of undersea volcanic areas. New ocean crust was (and is) forming along the mid-ocean ridges (Figure 3-33).

Mountain belts and stable cratons
Fig. 3-31. Map of the world showing continental mountain belts (brown) and stable ancient cratons or "shield" regions (orange and red, the oldest rocks being red). Ocean bathymetry (in shades of blue) show mountain ranges (mid-ocean ridges) beneath the oceans.
Age of the seafloor
Fig. 3-32. Geologic and geophysical mapping show that the crustal rocks beneath the modern oceans are less that 200 million years, with the youngest rocks (and some actively forming) occur along mid-ocean ridges.
Mid Ocean Ridges
Fig. 3-33. Map showing the location of the world's mid-ocean ridges. These undersea mountain ranges are the longest on earth. Mid-ocean ridges (where new ocean crust is forming) is found beneath portions of all the world's ocean basins.
 
Chapter 3 Quiz Questions
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