Introduction to Earth Science

Chapter 7 - Earth's Structure and Plate Tectonics

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 essential information to understand the Theory of Plate Tectonics. The Theory of Plate Tectonics explains how the Earth’s surface is broken up into large plates of rock whose slow movements create earthquakes, volcanoes, and mountains, changing the way the Earth looks over geologic time.

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 7-2). 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. The solid earth has a central core (both solid & liquid), a mantle (mostly solid though capable of slow flow by heat convection), and the crust (solid). Oceans (hydrosphere), glaciers (cryosphere), and atmosphere rest on the surface of 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) involve processes that are far grander, operating both near and deep below the surface, and taking place gradually over long periods of time (in spans 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. 7-1. Nearly all geologic processes observed on Earth fit in some way into Plate Tectonics Theory.
Structure of the earth showing the asthenosphere
Figure 7-2. Structure of the Earth: crust, mantle, and core.

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 mostly composed of relatively low-density silicates minerals rich in aluminum. The crust is a comparatively thin outer skin that ranges from about 2 miles (3 km) thick at the oceanic ridges to 40 miles (70 km) under 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 higher-density silicates rich in iron and magnesium that extends to a depth of about 1800 miles (2900 km).
• Large portions can flow slowly and are near melting.

• The core is the innermost part of the earth is believed to be a magnetic iron-nickel rich sphere that consists of a 758 mile (1220 km) thick solid and very dense inner core that is overlain by 1400 miles (2250 km) of dense molten material in the outer core. The outer core is liquid, and heat convection here creates currents in the liquid metal that generate Earth’s magnetic field.

Structure of the Earth
Fig. 7-3.
Structure of the Earth showing more detail. Subdivisions on the left are based on composition, whereas the subdivisions on the right are based on physical properties. Note that the lithosphere encompasses both the crust and the upper part of the mantle.

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. Figure 7-3 illustrates the structure of the Earth highlighting the physical properties of the different layers.

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 60 miles (100 km) in thickness, but may be about 155 miles (250 km) or more thick beneath the older portions of the continents. The lithosphere is broken up into moving plates, and the movements of these plates are responsible for all the large-scale features observable on the surface—including ocean basins, continents, and mountain ranges. Because lithosphere is cooler than the underlying asthenosphere, and behaves in a more brittle manner. It is the region where all earthquakes take place.

Asthenosphere (weak sphere)

The term asthenosphere refers to a semi-fluid layer beneath the lithosphere (within the upper mantle), between about 60 to 400 miles (100-650 km) below the outer rigid lithosphere (oceanic and continental crust) forming part of the mantle. The asthenosphere, although solid, is very hot and pressure is great enough for material to be able to slowly flow vertically and horizontally. This enables sections of lithosphere to undergo movements associated with plate tectonics. Geologist use the term plastic to describe how hot solid materials, including rocks, can deform and flow slowly. Since rocks in the asthenosphere are hot, they will deform rather than fracture under pressure.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 7-3).

Mesosphere (or lower mantle)

This region is a rigid layer between the depths of about 400 to 1800 miles (650 km and 2900 km), but the rocks at these depths are very hot and capable of gradual flow. Heat from the core drives mantle convection.

Outer core:
As discussed in section 3.6, 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)

Iron-nickel meteorite
Fig. 7-4. 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
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

The sections that follow explore the types of information we can learn from these three methods.
International Space Station
Fig. 7-5.
Gravity can be precisely measured from orbiting satellites.

Magnetism measurements reveals the Earth's metallic core

Earth's magnetic field is believed to be formed by the convection of hot, molten iron in the outer core. There must be significant amounts of iron for Earth to have such a strong magnetic field (Figure 7-6).

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 probably because the field is generated by movements in the outer core.

Magnetic Reversals: The Earth’s magnetic field reverses, causing the locations of the north and south magnetic poles to switch. Magnetic reversals have 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). We think that the magnetic reversals are caused by shifting currents in the liquid metallic outer core.
Earth's magnetic field
Fig. 7-6. Earth's magnetic field extends from the core and far out into space.

Gravity Measurements

Gravitometers are 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. Orbiting satellites are pulled closer to Earth over regions of higher gravity.

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. Figure 7-7 shows variations in the Earth's gravitational field as revealed by satellite gravity measurements. The map shows that older and colder crust, such as under regions in the oceans, is denser (having higher gravitational attraction) than where new ocean crust is forming along mid-ocean ridges. Gravitation is less where the crust is less dense, such as beneath continental regions and where rocks are hotter (associated with regional volcanism).

Gravitational forces increase with increasing mass and decreases with distance. The greater the mass between to objects (such as moons or satellites orbiting planets), the greater the gravitational attraction. In addition, the closer two objects (such as moons and planets), the greater the gravitational attraction.
Gravity Anomaly Map
Fig. 7-7. NASA's gravity anomaly map shows subtle differences in the Earth's gravitational field in different portions of the world.

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

Earthquake Shadow Zones: Extensive study of shock waves of earthquakes and the global monitoring of underground nuclear bomb testing reveal 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. Zones of seismic wave shadows occur in the regions shown in Figure 7-8 between about 105° to 140° on the opposite side of the globe from a seismic shock. These shadow zones shows us that part of the Earth's core is liquid material (molten material). In contrast, the 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. 7-8. 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)
• The Moho is the boundary between the crust and the mantle. It separates less dense crustal rock from underlying denser mantle rock.
• 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.

The locations of the Moho, CMB, and Lehmann Discontinuity are shown in Figures 7-3.

Seismic wave data used to map the lithosphere

Earthquake data also reveals the location of major fault zones of the world (Figure 7-9). 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 mountains, valleys, and may other landscape features.
Earthquake map of the world
Fig. 7-9. 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 7-10). Heat in the Earth is produced by radioactive decay of unstable isotopes as well as heat left over from when the Earth formed billions of years ago in the solar system's nebula. Gravity-driven heat convection within the Earth is the conclusive power source driving plate tectonic motions.

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. In addition, as ocean crust forms and ages with time, it cools down and its density increases. This increase in density helps old ocean crust to sink back into the mantle in regions called subduction zones (discussed below).

Mantle convection
Fig. 7-10. Mantle convection is the driving force of movement in the Earth's lithosphere.
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 lithosphere related to tectonic activity. Heat from inside the Earth drives mantle convection (hot material rises, cool material sinks). The rise and fall of masses of 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 per year).

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 earthquakes that propagates as a shock waves through the Earth.

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

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 is the parts of Earth's lithosphere that underlies ocean basins. Oceanic crust is primarily composed of mafic rocks (rocks rich in iron and magnesium) and are more 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 is 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). Because felsic rocks are less dense than mafic rocks, continents tend to float higher in the asthenosphere; by doing so, they rise above sea level.

In general, rocks found within continental landmasses 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. 7-11. Isostasy: 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 less dense crust under mountain ranges than under oceans. As geophysical studies reveal, continental crust is typically thicker and less dense than ocean crust.


Isostasy 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 isostasy, 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 7-11). 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. 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 7-12). 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 7-3).

Geologic Examples of Isostasy

An iceberg floating on the ocean is a perfect illustration of isostasy (Figure 7-13). 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.

Isostasy also causes vertical movement of the crust. 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 7-14).

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.

Himalayas and Tibet
Fig. 7-12. Crustal thickening in the Himalayan Mountains and Tibetan Plateau is illustrated in this photograph from space.
An iceberg illustrates isostasy.
Fig. 7-13.
Iceberg showing isostasy. 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-14. Isostatic rebound caused by the melting of continental glaciers reveals the fluid-like behavior of the asthenosphere.

Isostasy and the Age and Evolution of Continental Landmasses

Many hypotheses were put forward to try to explain the evolution of landscapes—isostasy 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 7-24 below). 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 7-15). The erosion of material from continental region contribute mass to the submerged regions along continental margins. In many regions along the continental margins the weight of additional sediments are casing them to sink (such as near the mouth of rivers, such as the Gulf Coast near the Mississippi River delta).

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 isostasy over time compared with youthful, mature, and old age landscapes
Fig. 7-15. Isostasy and the hypothesis of landscapes evolving through "youthful," "mature" and "old age" stages. Evolution of a landscape over time involves uplift, erosion, and isostasy.

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 that go back several centuries. Highlights include:

• Early Maps of the World: Maps compiled by early global explorations resulted in the observation of the matching shapes of the coastlines 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 7-16). As we will see in the next chapter, the volcanoes of the Ring of Fire relate directly to Plate Tectonics Theory.

Continental Drift

The Continental Drift Hypothesis was a prelude to the modern Plate Tectonics 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. More importantly, the drift hypothesis was supported by similarities of fossils, rocks, and mountain belts on both sides of the Atlantic, as explained further below.

Wegener's hypothesis was that all the observable continents bordering the Atlantic and Indian Oceans had once assembled into a single supercontinent that he named Pangaea. He determined that this great landmass began to break apart about 200 million years ago (Figures 7-17 to 7-19). He said that these continents started moving about 200 million years ago (MYA) and they are still moving. This is amazing because Wegener proposed this more than 100 years ago and it remains correct today. However, the theory was rejected by most scientists at the time.

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 continents separated and gradually migrated into their current configuration.

Geologic and fossil evidence 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.

Fossil evidence supporting Continental Drift includes:
• Similar fossil sites occur on different continents, when Pangaea was together. Examples include Mesosaurus and Glossopteris fossils (Figure 7-18). 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. This is because continents drifted from one climate zone to another, carrying fossils with them.
• 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, sea water flooded in creating the North Atlantic ocean basin.
• Finally, it opened completely to the open ocean to the south.
• This occurred between 60 and 100 million years ago.

• Similar processes are occurring in the African Rift Zones and Red Sea region today!

Rig of Fire
Fig. 7-16. The Ring of Fire is a zone of volcanoes, numerous earthquakes, and offshore deep trenches.
Fig. 7-17. Geographers noted that the continents fit together like a jig-saw puzzle.
Pangaea fossils
Fig. 7-18. Fossil evidence connecting lands of Pangaea about 260 million years ago)
Plate Motion
Fig. 7-19. The formation and breakup of Pangaea over 300 million years.

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 had relatively little volcanic or earthquake activity in other regions. 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 7-26). In most places around the Pacific Rim's 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 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 continents 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 solid, so it was difficult to formulate a mechanism for continental drift.

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.

(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 they reflect off the seafloor. Sonar investigation revealed the extent of the Mid-Atlantic Ridge in the center of the Atlantic Ocean basin (Figure 7-20).

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 5-30). 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's 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 (Figure 7-21).
Map of the Atlantic Basin
Fig. 7-20. Seafloor bathymetry of the Atlantic Basin (first mapped with SONAR), The scientific community at the time this map was astounded that the map data showed the existence of the Mid-Atlantic Ridge, a submarine mountain chain in the middle of the Atlantic Ocean.
Earthquakes under Japan reveal a pattern.
Fig. 7-21. Earthquakes under Japan revealed a pattern named a Benioff-Wadati Zone. This signature of earthquake data led to the recognition of subduction zones associated with deep ocean trenches and the origin of volcanic island arcs (like Japan) [discussed in more detail below].

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 7-6). 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 detect and measure the strength of magnetic fields) were used in World War II to search for submarines. It was noted from these investigations that the seafloor preserved large magnetic anomalies that lined up parallel the Mid-Atlantic Ridge (Figure 7-22). 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.

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 a certain temperature (called 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 7-23). With decades of studies of paleomagnetism of seafloor rocks and volcanoes around world the chronology of magnetic reversals through geologic time are now well known.

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 spreading 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. Because the Earth's magnetic field is reversing frequently through geologic time, the rocks forming and moving away from spreading centers preserve the pattern of preserved magnetic orientation. This pattern turns out to be mapable (Figures 7-22 and 7-23).

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 Figures 7-9, 7-20, and 3-25 below). 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. 7-22. 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. 7-23. 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 rocks of the ocean floors are much younger than the rocks of the continents

In the late 1940's methods of radiometric-age dating were developed. After WW2, samples of ocean crust and sediments were collected from the sea floor throughout the world ocean basins and analyzed using both radiometric-age dating (decay of 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 7-24).

  • The oldest ocean crust is about 200 million years (Figure 7-25) 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 7-24 to 7-26, 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 7-24).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 7-25 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 7-26). In contrast, old ocean crust is sinking back into the mantle or being added onto some continental margins.

Mountain belts and stable cratons
Fig. 7-24. 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. 7-25. 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. 7-26. 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.
Over time, the newly formed ocean crust cooled and moved slowly away from the mid-ocean ridges (Figure 7-2). These areas where new crust is forming and moving apart are called spreading centers. New ocean crust forms and moves away from spreading centers over time (Figure 7-3). Since new ocean crust is forming, old crust has to be disappearing somewhere, and it turned out that the old crust was sinking back into the mantle along extensive fault zones associated with the deep ocean trenches. These great fault systems are called subduction zones (illustrated in two plate-tectonics models, Figures 7-27 and 7-28). Subduction zones are locations where cool and dense ocean crust sinks back into the mantle (asthenosphere), as it sinks it heats up. Water and gases trapped in the sinking crust cause partial melting (forming magma) which rises (due to its lower density through zones of weakness in the lithosphere. Some of this rising magma accumulates in magma chambers, whereas some of it may actually rise all the way to the surface to form volcanoes. Earthquakes caused by friction along the subduction zone reveal that crust is slowly sinking back into the mantle.

Figure 7-29 is a map of Earth's lithospheric plates (the inferred plate boundaries around the world). Figure 7-27 illustrates the basic components of the plate tectonics model. These diagrams illustrate where new crust is forming along spreading centers along mid-ocean ridges, and where old ocean crust is being destroyed or recycled into new continental crust along subduction zones. Spreading centers and subduction zones are mapped as plate boundaries (see Figures 7-29). However, other features are also considered plate boundaries where crust is neither forming or being destroyed, but are rather moving past each other or crushing into each other. These regions have earthquakes but little or no volcanic activity. Examples where this is taking place include the San Andreas Fault in California (a strike-slip fault plate boundary) and the Himalayan Mountains between where India and Tibet are crashing into each other (discussed below).
Lithospheric plate boundaries illustrated
Fig. 7-27. Plate tectonic model
Plate tectonics model showing types of plate boundaries
Fig. 7-28. A simplified model of plate tectonics showing types of lithospheric plate boundaries.
In 1962, a classic paper written by Harry Hess (a geologist and Navy submarine commander during World War II) who described that the continents did not plow through the oceanic crust (as proposed by Wegener's [1915] Continental Drift Theory), but instead, proposed that they were riding with the oceanic crust like a conveyor belt. This idea was combined with the works of others including: Vine and Matthews (1963) (see Figure 3-23), and Tuzo Wilson (who first reported his theory about the origin of plate boundaries in the early 1960s). Many any other contributions from scientists around the world to put the Theory of Plate Tectonics together.

Plate Tectonics Theory

Today, Plate Tectonics Theory explains the large-scale motions of Earth's lithosphere. Plate tectonics theory builds on concepts of Wegener's Continental Drift Hypothesis. It was the global efforts of seafloor exploration following World War II resulted in the development of seafloor spreading theories in the late 1950s and early 1960s. This exploration effort involved perhaps many thousands of scientists within the "global geoscience community" (geologists, oceanographers, paleontologists, and geophysicists, assisted by world leaders) who systematically gathered information and mapped the world, both on land and underwater. The mechanics of Plate Tectonics Theory were largely resolved as large quantities of data about the age and distribution of rocks beneath the ocean basins were compiled from ocean drilling programs and geophysical studies of the ocean crust from around the world. Seafloor mapping, along with the study of volcanoes and earthquakes provided the evidence to support plate tectonics theory.

Plate Tectonics Theory helps to explains to some degree almost all things geological in the observable world, past and present. Plate tectonics expounds that Earth’s outer shell (lithosphere) is composed of several large, thin, relatively rigid plates that move relative to one another (Figure 7-29). Movements along fault systems that define Lithospheric plate boundaries produce most observed earthquakes.

Map of lithospheric plates and plate boundaries around the world
Fig. 7-29. Map showing the location of lithospheric plates and plate boundaries of the world. Boundaries shown in yellow are divergent boundaries, Those in orange are convergent boundaries. Note that some plates include both continental and oceanic crust.
Watch a video about the Pacific Ring of Fire and Its Earthquakes (and Volcanoes) (YouTube video)

Three Types of Lithospheric Plate Boundaries

There are general types of lithospheric plate boundaries (see Figures 7-27 to 7-29).

Divergent boundary
(where plates are pulled apart by tensional forces)—When plates diverge, spreading centers form creating new oceanic crust. Examples include mid-ocean ridges in world's ocean basins. Spreading centers occur where continents are pulling apart. Examples include the Africa rift zones, Red Sea basin, Iceland, and North America's Great Basin region including the Gulf of California (see discussions below).

Convergent boundary (where plates are pushed together by compressional forces)—When lithospheric plates collide... mountains belts form - examples include the Himalayas, Alps, and ancient Appalachian Mountains when the ancient continent of Pangaea formed. When continents collide with ocean crust... subduction zones with deep ocean trenches and volcanic arcs form - examples include the Andes Mountains, Aleutian Islands, Japan, Philippines, Indonesia, the ancient Sierra Nevada and modern Cascades Range in northern California, Oregon, and Washington.

Transform boundary (where plates slide past or are rotational)—When plates slide past each other creating fault systems along plate margins. Examples include the San Andreas Fault in California and major faults in Pakistan, Turkey, and along the Jordan River/Dead Sea.

Divergent Plate Boundaries

Divergent plate boundaries are locations where tensional forces are pulling things apart. In locations where lithospheric plates are diverging, the rates of divergent motion range from 2 to 17 cm/year.

Spreading Centers along Divergent Plate Boundaries

A spreading center is a linear area where new crust forms where two crustal plates are moving apart, such as along a mid-oceanic ridge. Spreading centers are typically seismically active regions in ocean basins and may be regions of active or frequent volcanism (Figure 7-30). Spreading centers are associated with divergent plate boundaries.

Iceland is host to an active spreading center that is exposed above sea level (Figure 7-31).
Spreading center along a mid-ocean ridge Iceland's Rifts
Fig. 7-30. Formation of new oceanic crust along a spreading center associated with a mid-ocean ridge. Some spreading centers appear on land. For example, a portion of the Mid-Atlantic Ridge is exposed on Iceland. Fig. 7-31. Iceland's is an exposed portion of the North Atlantic spreading center. Iceland is splitting along a rift zone where new crust is forming. Of 130 volcanoes on the landmass, 30 are currently considered active.

Seafloor spreading and formation of new ocean crust

Seafloor spreading features and processes include:
• Involves oceanic crust (OC) only.
• Tensional forces pull oceanic crust apart (forming faults that split deep into the newly forming ocean crust).
• This forms a mid-oceanic ridge (MOR).
• Volcanic activity along faults and fracture zones allows magma to rise cool on or near the seafloor surface.
• This volcanic activity generates new seafloor/oceanic crust,
• New oceanic crust moves away from spreading center as more is formed.
• Youngest oceanic crust is found near the ridge, oldest (and colder)crust is far away from ridge.
• Uplifts occurs as it is rifted, so MORs are the shallowest part of deep ocean basins.
• The MOR is symmetrical about the ridge.
• Magnetic reversals preserved in volcanic rocks are found along MORs worldwide.
• Marine sediments deposited on top of new ocean crust thicken away from the ridge as crust grows progressively older.
• Hydrothermal vents (ie: vents of hot water

called "black smokers") are found in spreading centers.

Ocean Rises vs. Ridges

Spreading center are active at different rates, resulting in different physical characteristics.
A rise spreads faster and is less steep, a ridge is steeper and spreads slower.
East Pacific Rise (see Figures 7-25, 7-29, and 7-32)
Mid-Atlantic Ridge (see Figures 7-25, 7-29, and 7-30).

• On Iceland, the MOR rises to the land surface, its rate of spreading is about 15 cm/yr (Figure 7-31).

East Pacific Rise
Fig. 7-32. The East Pacific Rise is a rapidly forming spreading center (a mid-oceanic ridge that separates the Pacific Plate to the west from (north to south) the North American Plate, the Rivera Plate, the Cocos Plate, the Nazca Plate, and the Antarctic Plate. See Figure 7-29.

Continental Rifting

Continental Rifting occurs where divergent boundaries form within continental landmasses:
• Involves rifting (pulling apart) of continental crust (CC) only.
• Forms possibly from convection in the asthenosphere
• Large amounts of sediments are usually produced in continental rifting zones.

• Initially, when a continental rift forms it has continental processes such as the formation of large lakes, rivers, and beaches. Later, as it pulls farther apart it can become an oceanic rift when sea water floods in. It then becomes a MOR.

Present continental rifts include:
Red Sea and East African Rift System (Figure 7-33 and 7-34).

• The breakup of Pangaea began with continental rifting starting about 200 million years ago with Africa pulling apart from North and South America. It eventually flooded with seawater and became the new Atlantic Ocean Basin.
Continental rifting along the Sinai Peninsula
Fig. 7-33. Continental rifts along the Red Sea and Sinai Peninsula (Jordan River, Dead Sea)
African rifts
Fig. 7-34. Africa rift zones are zones where the African continent are being pulled apart. The African Rift basins are spreading centers that are the location of large inland lakes and much volcanic activity. One day in the distant future become seas like the modern Red Sea.

Crustal Extension and Continental Rifting

Crustal extension occurs where a divergent plate boundary develops under a continental landmass on a large scale, associated with continental rifting (Figure 7-35).

Both crustal extension and continental rifting are occurring in northern Gulf of California and throughout North America's Great Basin region under Nevada, Arizona and eastward into the Rio Grand River rift valley in New Mexico (Figure 7-36). As the Atlantic Ocean opened, the North American continent was pushed over a spreading center that is now the entire region of Utah, Nevada, Arizona, and parts of New Mexico. Baja California and the Peninsular Ranges of San Diego and Orange counties have been rifted away from the Mexican coastline gradually over about 23 million years. Baja will continue moving northward, eventually crushing into southern Alaska in the distant future!
Crustal extension and compression
Fig. 7-35.
Crustal extension and crustal compression.
Gulf of California
Fig. 7-36
. Gulf of California and Great Basin—a region where crustal extension is occurring.

Convergent Plate Boundaries

Convergent Plates move together and collide so you have compressional forces. They are associated with active margins—locations where mountain building is occurring, resulting in numerous earthquakes and andesite (explosive) volcanoes.

A subduction zone is a plate boundary along which one plate of the Earth’s outer shell descends (subducts) at an angle beneath another (Figure 7-37). A subduction zone is usually marked by a deep trench on the sea floor. An example is the Cascadia Subduction Zone offshore of Washington, Oregon, and northern California (see Figure 7-19 below). Most tsunamis are generated by subduction-zone-related earthquakes.

Figure 7-37 illustrates how earthquake data reveals the geometry of a subduction zone. This diagram show the location and intensity of earthquakes over a period of time in the vicinity of the Tonga Islands in the South Pacific Ocean. A deep ocean trench runs along the southeast side of the island chain. Earthquake data shows that a major fault system descends at an angle, extending eastward beneath the Tonga Island and extends of hundreds of kilometers at a steep angle deep into the upper mantle (asthenosphere) where it is presumed that earthquakes cease because rocks are too hot and under intense pressure that it easier for them to fold and flow plastically than to fracture as brittle rock. The earthquake data suggests that the eastern edge of the Australian Plate is being over run by the western edge of the Pacific Plate, and that rocks of the Australian Plate are descending into the upper mantle.
Earthquakes reveal geometry of the Tonga subduction zone
Fig. 7-37. Earthquake data reveals the geometry of a subduction zone in the region of Tonga.

Three types of Convergent Plate Boundaries: OC/CC, OC/OC, & CC/CC

Three types of convergent plate boundaries are recognized: .
a) Subduction of ocean crust (OC) beneath continental crust (CC)
b) Subduction of ocean crust (OC) beneath ocean crust (OC)
c) Continental Collisions: continental crust (CC) colliding with continental crust (CC).

a) Subduction of ocean crust (OC) beneath continental crust (CC).

• Denser, thinner OC is pushed or subducted beneath less dense and more buoyant CC.
• A chain of volcanoes formed, called a continental volcanic arc.
• Subduction produces both deep and shallow focus earthquakes (with tsunami potential); the largest ever--9.5 magnitude in Peru/Chile Trench in 1960.
• Volcanoes of the andesite (explosive) type. Examples include the Andes and the Cascade Range , etc.
• Deep trenches form around continents margins. Trenches are especially well developed in regions far away from spreading centers (where the ocean crust is old, cold, and denser, and therefore sinks more rapidly).
• Subduction reduces amount of (and destroys) OC.
• Rates of subduction are up to 15 cm/yr in the active margins of the Pacific Basin.

• Andes in South America (Figure 7-38)
• Cascades in United States (include such volcanoes as Mt. St. Helens, Mt. Rainier, Mount Shasta, Crater Lake and many others)
subduction zone
Fig. 7-38. Subduction zone geometry (OC/CC) is revealed by the location of earthquakes and volcanic activity. Subduction zones are where oceanic crust is destroyed and new continental crust forms. Subduction zones associated with ocean trenches surround much of the Pacific Ocean Basin.

b) Subduction of ocean crust (OC) beneath ocean crust (OC).

• Many similar features as above [OC/CC].
• Denser, older, cooler OC is pushed or subducted beneath less dense, warmer, younger OC.
• Forms island volcanic arcs.
• Deep and shallow (tsunami potential) focus earthquakes
• Volcanoes not as explosive as above with OC/CC, as there is no mixing of CC rocks (called granites). Volcanic rocks are mostly basaltic in composition.
• Subduction reduces amount of (destroys) OC.


Japan, Tonga Islands, and Aleutian Islands (Alaska)(Figures 7-39 and 7-40)
Aleutian Island chain and trench
Fig. 7-39.
Aleutian Islands and Aleutian Trench.
Aleutian volcanoes
Fig. 7-40.
Volcanoes of the Aleutian Islands volcanic arc.

c) Continental Collisions: continental crust (CC) colliding with continental crust (CC)

When continents collide with other continental landmasses:
• Neither of the CC are subducted,
• Both are very buoyant and want to "float" or ride high.
• This is where you form the very large mountain chains.
• Mountain building occurs with lots of earthquakes; massive erosion also occurs.


Himalayas (India) beginning 45 million years ago) (Figure 7-41)
Alps Mountains are being pushed up by collisions between Africa (and Italian Peninsula) with Europe.
Appalachians Mountains in the eastern United States (formed when North America collided with Africa about 350-400 million years ago (before the Atlantic Ocean opened later).
Tibetan Plateau
Fig. 7-41. Migration of "India" away from ancient Pangaea has led to the collision of continental land masses resulting in the rise of the Himalayan Mountains. In this region, the continental crust on both sides of the plate boundary are too light to sink into the mantle.

Transform Boundaries

Transform boundaries are locations where one plate is sliding past another.
• Can occur in any crustal type (OC or CC)
• Crust is neither produced or destroyed

Continental Transform Faults

• In continental crust, transform faults can be large destructive faults like the San Andreas Fault System in California (Figure 7-42).
• Earthquake magnitudes up to 8.5 have been measured.
• Rates on the San Andreas Fault (SAF) average 2-5 cm/yr or LA will be adjacent to SF in about 20 million years!
• Compression(and uplift) or tension (and down-warping) can occur. The high mountains in Southern California are a result of this kind of compression along the SAF including the San Gabriels, San Jacinto, and San Gorgonio Mountains.

Oceanic Transform Faults
• In ocean crust, smaller transform faults occur perpendicular to the spreading centers.
• They have smaller earthquakes associated with them, when compared with their continental cousins.
• These faults occur where there is a bend or change in the rate of spreading along the MOR.

Western North America Plate boundary
Fig. 7-42. The San Andreas Fault system is part of a complex transform plate boundary along the West Coast of North America.

Review: Examples of Plate Boundaries

Convergent boundaries Divergent boundaries Transform boundaries
When continents collide mountains belts form. Examples:
  • Himalayas
  • Alps
  • ancient Appalachian Mountains
When plates diverge, spreading centers form creating new oceanic crust. Examples:

  • mid ocean ridges in world's ocean basins
  • The African Rift Zones and the Red Sea
  • The Great Basin and Rio Grande Rift Zone
When plates slide past each other creating fault systems along plate margins. Examples:
  • San Andreas Fault
  • Pakistan
  • Turkey
  • Jordan River/Dead Sea
Convergent boundary along Hinalayan Mountains Divergent boundary of Mid Ocean  Ridge in Iceland San Andreas Fault in Central California
Fig. 7-43. Himalayan Mountains are a convergent plate boundary Fig. 7-44. Mid Ocean Ridge in Iceland is a divergent plate boundary Fig 4-45. San Andreas Fault system is a transform plate boundary
When continents collide with ocean crust
trenches with subduction zones and volcanic arcs form - examples:
  • Andes Mountains
  • Aleutian Islands
  • Japan, Philippines, Indonesia, etc.
  • Ancient Sierra and modern Cascades
Spreading centers occur where continents are pulling apart. Examples:
  • Africa rift zones
  • Red Sea
  • Iceland
  • North America's Great Basin
Transform faults also occur within plates, but are related to movements that shape the seafloor. Examples:
  • Dead Sea fault zone, Jordan
  • India/Pakistan boundary fault
  • North Anatolian Fault, Turkey
South America plate boundar Divergent boundary forming in the Red Sea fransform faults on the seafloor; North American western plate boundary
Fig. 7-46. Convergent boundary along the west coast of South America Fig. 7-47. A divergent boundary forming in the Red Sea area Fig. 7-48. Transform fracture zones offshore of California are within the Pacific Plate

Continental margins may or may not be plate boundaries! For example, the East Coast is in the middle of the North American Plate. Why? When North America first split away from Africa and Europe, there was first a continental rift valley; it became a plate boundary between the three expanding lithospheric plates. As new crust formed along the Mid Ocean Ridge spreading center, it became attached to the plates on either side. Today the North American Continent is part of the larger North American Plate! (See Figure 7-29.)

Hotspots and Mantle Plumes

A hotspot is a place in the upper mantle of the Earth at which extremely hot magma from the lower mantle upwells to melt through the crust usually in the interior of a tectonic plate to form a volcanic feature.
• These are hotspots beneath the lithosphere caused by rising plumes of hot mantle material.
• Can form volcanoes on surface (examples include Hawaii and Yellowstone hotspots (Figures 7-49 and 7-50).
-Volcanoes are mostly mafic (basaltic) as these lavas are very hot and very fluid from deep sources.
-Less common are felsic (rhyolitic) magmas as they are thicker and less prone to flow.
• Hotspots can occur beneath any crustal type (OC or CC).
• Where they form a trace consisting of a chain of volcanoes (like in Hawaii's Emperor Seamount Chain, Figure 7-49)
• Hotspots can exist in about the same place for 10's of millions of years
• The Hawaiian Hotspot has existed for about 60 million years; the youngest part of the Emperor Seamount Chain.
• The oldest part of the Emperor Seamount Chain has already been subducted (destroyed).
• There are hundred of hotspots located around the world. Some are larger and more active than others.
• Most hotspots are located under the interior sections of lithospheric plates, but some occur near divergent plate boundaries.
• Paleomagnetism in rocks on the ocean floor associated with hotspots provides a method for determining speed and direction of plate motions.
• We are not sure of the exact mechanism that forms hotspots, there are some ideas (see below).

Yellowstone National Park Hotspot:

• The Yellowstone hotspot currently under continental crust (Figure 7-50).
• Yellowstone is a very large and complex supervolcano.
The Yellowstone supervolcano is at the eastern end of a long chain of progressively older supervolcanoes that formed along the trace of the Snake River Plain (Idaho, Washington, and Oregon)
• The hotspot had formed volcanoes of both basaltic and rhyolitic composition.
• Has had large rhyolitic eruptions 3 times in the last 2 million years
• This hotspot appears to have been present for less time than the Hawaiian hotspot (about 17 million years).

Hawaii Hotspot and the Emporer Seamount Chain
Fig. 7-49.
Map of the Hawaiian Hotspot and the Emperor Seamount Chain in the Pacific Ocean basin.

Migration of the Yellowstone Hotspot under western North America
Fig. 7-50
. The Yellowstone Hotspot is beneath the North America continent and is slowly migrating eastward as the continent is moving westward.
Hot topic: Are hotspots related to "astroblemes" (large asteroid impacts)?

Earth has been hit by many asteroids throughout the geologic past. If Earth didn't have an atmosphere and active plate tectonics it would appear heavily cratered like the moon!

Current research suggests that massive asteroid impacts can deeply penetrate and fracture the lithosphere, allowing craters to flood with lava—the magma generated by both the impact and material flooding upward to the surface from deeper down. The question is, do astroblemes turn into hotspots? Also, it has been suggested that shock waves from a massive impact can travel through the Earth and will concentrate energy at the "antipoles" - resulting in deep fracturing of the lithosphere, resulting in massive volcanic eruptions. Examples of two possible "antipole" eruptions include the formation of the Deccan Traps in India (opposite the K/T boundary impact ~66 million years ago in the Yucatan region of Mexico. Another massive flood eruption occurred about 250 million years ago, forming the massive Siberian Traps (massive flood basalts that formed about the time of the great end-of-Permian extinction).

What drives plate motions?

• Researchers agree that convective flow in the mantle is the basic driving force of plate tectonics (Figure 7-51).

Forces that drive plate motion:

Slab-pull - the slow pull of mantle material where is moves from a rising location to a sinking location.
• Slab-suction - The high density of cold ocean crust sinking into the mantle pulls crust with it.
Ridge-push - new ocean crust is warm and tends to rise above the ocean floor, pushing older cooler crust away

Plate tectonics model explains many aspects of the geometry of continents and ocean basins and the processes creating new oceanic and continental crust. Material that does not become incorporated into the lithosphere sinks and becomes incorporated back into the mantle.

Importance of plate tectonics

• The theory provides explanations for many of earth’s major processes
• Explains the geologic distribution of earthquakes, volcanoes, and mountains
• Explains the distribution of ancient organisms and mineral deposits
• Plate tectonics are responsible large volumes of oil and gas deposits we enjoy today. Think about how your life and society would be different if we only had a mere fraction of the hydrocarbons we currently have and use.
Forces that drive plate tectonic motion
Fig. 7-51. Mantle convection is the driving force of motion of lithospheric plates. Much of the convection motion may be in the upper mantle, but it is likely to extend deep into the earth's molten outer core.
How does Plate Tectonics explain why continental landmasses are so old (compared to ocean crust)?

The interior of the earth is very hot—the source of this heat is thought to be left over from the formation of the planet several billion years ago. As shown in Figure 7-51, the combined effect of the internal heat of the Earth and the force of gravity drive convection currents within the Earth . Heat things up, they expand, become less dense, and the material rises. Cool things down, they condense, increase in density, and the material sinks. This can be easily demonstrated the way hot air balloon rise and fall, or the way currents move when water is heated, or the way currents within a boiling pot of soup rises and sinks when it cools (Figure 7-52).

When new ocean crust forms in spreading centers, it is still hot for a time, but it eventually cools by having contact with the cold, deep ocean waters. As a result, old ocean crust is enriched in dense minerals. As it ages, it also absorbs water from the ocean and is becomes blanketed with marine sediments. Where subduction takes place, cold, dense ocean crust sinks back into the mantle. However, as the old crust sinks, it heats up and some of the materials within it melts (assisted by the presence of water and other gases). The materials that melt rise as hot fluids (magma and gases) through the overriding continental crust, forming large magma filled chambers that eventually crystallize into rock at depth, some of which erupts at the surface to form volcanoes. The new rocks that form along the continental margins are less dense than the original oceanic crustal rocks, therefore they eventually iso statically float and rise above the ocean surface, becoming land. Over time, more and more of this lighter rock accumulates first forming volcanic island chains. These volcanic arc and the sediments they shed eventually becomes scraped off and crushed onto the margin of continents—often pushed up as coastal mountain ranges. It this manner, continents grow slowly around their margins in a process called accretion. This process explains why the oldest rocks occur in the shield regions of continents and younger material occurs along continental margins.

Continental Accretion

Accretion is a process by which material is added to a tectonic plate or a landmass. This material may be sediment, volcanic arcs, seamounts or other igneous features, or blocks or pieces of continental crust split from other continental plates (Figure 7-53 to 7-54). Over geologic time (measured in millions of years), volcanic arcs form and may be crushed onto (or between) colliding continents along plate boundaries. Pieces of continental land masses may be ripped away and carried to other locations. For instance, Baja California and parts of southern California west of the San Andreas Fault are being ripped away from the North American continent and are slowly being carried northward. These rocks may eventually pass what-is-now San Francisco, and perhaps 70 to 100 million years from now will be crushed and accreted into the landmass currently known as Alaska!

The entire West Coast of North America is made up of massive fault-bounded blocks of crust (called terranes).A terrane is a fault-bounded area with a distinctive stratigraphy (collection of rocks), structure, and geologic history compared with surrounding terranes or land masses.
Boiling pot of soup
Fig. 7-52. Currents in boiling soup demonstrates convection. The "broth" rises, cools, and sinks (like the formation and destruction ocean crust over time). In contrast, the bubbly "froth" builds up in patches over where cool soup sinks back into the pot. The buildup of froth in patches is similar to the way continents build up over time.
Another YouTube video:
Continents Adrift An Introduction to Continental Drift and Plate Tectonics
This video explains much of what this chapter reviews.
Plate Tectonics Fig. 7-53. Plate tectonic model: Subduction introduces oceanic crustal rocks (including sediments) back into the asthenosphere. Water and gas helps low-temperature minerals to melt and rise as, forming new continental crust (less dense than oceanic crust). Floating on the Asthenosphere, the continental crustal materials accumulate, forming continents. Subduction is a refining process Fig. 7-54. The processes associated with subduction lead to the accretion (growth) of continents over time. As ocean crust is recycled back into the upper mantle, the lighter material accumulates near the surface along continental margins. Pieces of lithosphere are sometimes scraped off one plate and crushed onto and added (accreted) to another plate.
Fig. 7-55. Terranes in the San Francisco Bay area. This cross section of the Santa Clara Valley (south of San Jose, California) shows several fault-bounded terranes. Each of the large crustal blocks formed in locations far south of the Bay Area, but have gradually moved north along the fault system that bifurcates through the region. Over time, California has formed (assembled) by the accretion of terranes (small crustal landmasses) carried in by plate-tectonic processes slowly over geologic time. Cross section of the San Francisco Bay area

Ancient Parts of Continents: Cratons and Shields

A craton is a part of a continent that is stable and forms the central mass of the continent. The craton region of North America includes the region between the Rocky Mountains (to the west) and the Appalachian Mountains (to the east) and include the Canadian Shield.

A shield is a large area of exposed Precambrian-age crystalline igneous and high-grade metamorphic rocks that form tectonically stable areas. In all cases, the age of these rocks is greater than 570 million years and sometimes dates back 2 to over 4 billion years. For instance: the Canadian Shield is part of the North American craton region. Shallow inland seas have flooded over and retreated from North America's craton/shield region in the past billion years.
World Physiographic Provinces Avalon Formation and Breakup of Pangaea

Through geologic time new continental crust forms and accumulates along the margins of continents. The "floating" continental crust eventually crashes into other land masses, and these terranes may assemble into larger continental crustal plates. For instance, the formation of the ancient supercontinent Pangaea assembled through continental accretion. Pangaea later gradually split apart by continental rifting forming the world's continental landmasses that exist today. The geologic story of the formation and breakup of Pangaea are preserved in the rock record all along the Atlantic Margin of North America, Europe, and Africa.
Breakup of Pangaea in the New Jersey region along the Atlantic Coastal Margin
Fig. 7-56. Continental shields and cratons
Continental shields contain the oldest rocks preserved in the cores of continental landmasses. These regions formed by processes associated with continental accretion billions of years ago, long before the continents of the modern world existed. These ancient shield are part of the stable parts of continents (cratons) and in many places are partially covered by younger sedimentary rocks (such as in the Great Plains and Midwestern Low Plateau regions of North America).
Fig. 7-57. Formation of Pangaea by closing of the "proto-Atlantic" Iapetus ocean about 300 million years ago. Fig. 7-58. Breakup of Pangaea and formation of the Atlantic Ocean about 200 million years ago.
California Geology and Plate Tectonics History
California has been one of most studied geologic region of the world, and for good reasons: earthquakes!

Through its history, California has transitioned from a passive continental margin (before the breakup of Pangaea) to an active margin with the transition to subduction zone activity and the formation of the Cordilleran volcanic chain (during the Mesozoic Era). The Cordilleran Ranges is name for the volcanic arc that formed the Sierra Nevada Range and the Peninsular Ranges extending south in to Baja California). Subduction ended when the ancient Farralon Plate was overrun as North America moved westward, overriding the nothern end of the spreading center in the Eastern Pacific basin (Figure 7-62). This lead to the formation to the modern transform plate boundary associated with the San Andreas Fault (part of the greater California fault system) and the opening of the Gulf of California.

California Faults California earthquakes San Andreas Fault System in California
Fig. 7-59. Geologic map of California shows the complexity of the different regions within the state. Fig. 7-60. California earthquakes demonstrate that the region is an active margin Fig. 7-61. The San Andreas Fault System in California showing the locations impacted by major earthquakes.

Farollan Plate Assembling California:
California formed gradually over a billion years though processes involving subduction (forming island arcs) and by accretion (attachment of small land masses carried in for other parts of the Pacific Ocean basin). Before the opening of the Atlantic Ocean Basin, California was sometimes a passive margin.
Information about the geologic evolution of California:

Geologic History of Central California

A technical report about the San Andreas Fault System:

Wallace, Robert E., 1990, The San Andreas Fault System, California: U.S. Geological Survey, 283 p.

This historically significant report provides an overview of the history, geology, geomorphology, geophysics, and seismology of the most well known plate-tectonic boundary in the world.

Generalized California Plate Tectonic History:

No rocks older than ~1 billion years exist in CA - all more ancient materials in the CA region were subducted or moved elsewhere...

~1 billion to ~250 million: CA was a mostly a passive margin or was accumulating as sediments on an actively migrating seafloor. Periods of mountain building and other plate-tectonic-related activity moved small land masses along the West Coast region. North America moved westward and northward over time.

~250 to ~30 million: subduction and island-arc volcanism dominated the CA coast. An ocean trench existed along where the coast exists today, and a subduction-related igneous activity created the great volcanic arc formed the core of the Sierra Nevada

~30 years ago to present: the San Andreas Fault System began to modify the coastline - transform faulting replaced subduction

. Baja California split away from the Mexico. Uplift and erosion has exposed the core of the ancient volcanic arc, now exposed throughout the Sierra Nevada and Peninsula Range (Baja and San Diego region).
Fig. 7-62. Formation of the San Andreas Fault caused by North America Plate overriding the ancient Farallon Plate. Remnants of the Farallon Plate exist as the Juan de Fuca Plate (offshore Oregon & Washington) and the Cocos Plate (off central America).

Supporting evidence of long-distance movement along the San Andreas Fault System.
Pinnacles volcano California Rocks California conglomerate
Fig. 7-63. The Pinnacles Volcano originally formed near Los Angeles nearly 23 million years ago. The western half (Pinnacles Formation) is now about 215 miles [350 km] north of the eastern half (Neenach Formation). Fig. 7-64. Granitic basement rocks in the Coast Ranges originally formed as part of an volcanic arc complex in the Mesozoic Era. They were ripped off of SoCal and carried northward by plate tectonics motion. Fig. 7-65. Cretaceous-age gravels deposited by an ancient river system in southern California were carried northward from their source area and are now scattered throughout the Coast Ranges.

Recommend reading! Learn more about Plate Tectonics Theory at these online resources prepared by the Smithsonian Institution and U.S. Geological Survey:

This Dynamic Earth (The Story of Plate Tectonics) -
this on-line booklet is used for teaching plate tectonics at schools and universities around the world. It has a companion map:

This Dynamic Planet (World Map of Volcanoes, Earthquakes, Impact Craters, and Plate Tectonics

(see Figure 7-66).

Crustal age of the Seafloor Map: National Oceanic and Atmospheric Administration, National Geophysical Data Center [large image]
This Dynamic Planet
Fig. 7-66. Plate Tectonic Features Map from "This Dynamic Planet."
Field guides to the San Andreas Fault and other regional faults in the San Francisco Bay region.

Where’s the San Andreas Fault? A Guidebook to Tracing the Fault on Public Lands in the San Francisco Bay Region
Where's the Hayward Fault? A Green Guide to the Fault
Geology Field Trips To California's Central Coast
Chapter 7 Quiz Questions 7/18/2017