Global Tectonics

Global Tectonics

Introduction

Each rocky body, whether planet or moon, started with a hot interior.

Each has been kept warm over time by energy released by the decay of radioactive isotopes (同位素 ).

Despite radioactive heating, rocky bodies have cooled considerably since their formation, so that their outer layers have stiffened into lithospheres.

Introduction (2)

The interior of Earth remain hot

and geologically active.

The mantles of Earth lose internal heat by convection ( 對流 ), the slow flow of solid rock.

Hot rock rises upward to near the surface.

Earth’s stiff lithosphere is broken into a collection of near-rigid plates.

Introduction (3)

Most large-scale geologic events, like earthquakes or volcanic eruptions, originate within Earth’s interior.

Many other processes in the Earth system, such as the hydrologic and biogeochemical cycles, are profoundly affected by plate tectonics.

Plate Tectonics:From Hypothesis to Theory

Plate tectonics is a scientific theory that explains two centuries of often puzzling observations and hypotheses about our planet Earth.

The continents are drifting very slowly across the face of our planet.

Continental drift is a concept with a long history.

Plate Tectonics:From Hypothesis to Theory (2)

A century ago geologists puzzled over the fit of the shorelines of Africa and South America.

They noted that fossils of extinct land-bound plants and animals, glacial deposits, and ancient lava flows could be matched together along coastlines that today are thousands of kilometers apart.

Coal was found in Antarctica( 南極洲 ). Coal forms in tropical climates, implying that

Antarctica has moved in the past.


Faced with puzzling data, scientist developed hypotheses to explain them.

Alfred Wegener proposed the most comprehensive early hypothesis for “Continental Drift” in 1912.


His theory was widely rejected because:Ocean floor was too strong to be plowed aside.

Wegener had not proposed a plausible force that could induce the continents to drift.

Attempts to test Wegener’s hypothesis with observations had mixed success.


In 1960, the Theory of Plate Tectonics was born.Plate tectonics is the process by which Earth’s hot interior loses heat.

We can measure the slow drift of plates worldwide using satellite navigation systems.

The basic premises of plate theory are secure because they can be tested against a wide variety of observations.

What Earth’s Surface Features Tell Us

The rocks beneath our feet are solid, but they are not rigid.Topography: the relief and form of the land above sea level. Bathymetry: topography on the ocean floor.Earth bulges around its equator and is slightly flattened at the poles.All evidence points to centrifugal force caused by Earth’s rotational spin.

Isostasy (地殼均衡 ): Why Some Rocks Float Higher Than Others

The continents average about 4.5 km elevation above the ocean floor.They stand notably higher than the ocean basins because the thick continental crust is relatively light (average density 2.7 g/cm3).The thin oceanic crust is relatively heavy (average density 3.0g/cm3). The lithosphere floats on the asthenosphere.

Fig. 2.2

Isostasy (2)

The principle of isostasy governs the rise or subsidence of the crust until mass is buoyantly balanced.

Because of isostasy, all parts of the lithosphere are in a floating equilibrium.

Low-density wood blocks float high and have deep “roots,” whereas high-density blocks float low and have shallow “roots.”

Earth’s Surface: Land Versus Water

The ocean covers 71 percent of Earth’s surface.Land occupies only 29 percent.Sea level fluctuates over time.When climate is colder and water is stored as ice:

Sea level falls.The shoreline moves seaward.

When climate gets warmer:The ice melts.Sea level rises.The shoreline advances inland.

Fig. 2.3

Earth’s Surface: Land Versus Water (2)

Undersea mid-ocean ridges form a continuous feature more than 60,000 km long.

Mid-ocean ridges mark where two oceanic plates spread apart.

New lithosphere forms in the gap.

Passive margins have few earthquakes and little volcanic activity.


The continental shelf steepens slightly at 100-200 meters below sea level.The continental slope is the flooded continental margin.The continental rise descends more gently from the base of the continental slope.Earthquakes and volcanoes are common along active margins.

Fig. 2.5


Ocean trenches occurs where oceanic lithosphere and continental lithosphere converge at the boundary between two plates.

Because oceanic lithosphere is the denser of the two, it descends under the active continental margin and sinks into the deeper mantle.

The large, flat abyssal floors of the open ocean lie 3 to 6 km below sea level.

Fig. 2.6

What Earth’s Internal Phenomena Tell Us

Rocks are poor conductors of heat, so Earth moves its internal heat by moving the rock itself.

The circulation of hot rock is maintained by mantle convection.

Geothermal Gradients

A gradient is a progressive change in some physical or chemical property.

The geothermal gradient varies widely with geography from 5oC/km to 75oC/km.

Mantle Convection

Conduction is the process by which heat moves through solid rock.

Earth’s heat can move in a second process called convection.

Convection can happen in gases, in liquids, or, given enough time, in ductile solids.

A prerequisite condition for mantle convection is the thermal expansion of hot rock.

Fig. 2.7

Mantle Convection (2)

Rock expands as its temperature increases.

Its density thereby decreases slightly.

The hot rock is buoyant relative to cooler rock in its immediate neighborhood.

A 1 percent expansion requires an increase of 300-400oC and leads to a 1 percent decrease in density.

Viscosity is the propensity of rock to ductile flow.


Rock does not need to melt before it can flow.The presence of H2O encourages flow in solid rock.Convection currents bring hot rocks upward from Earth’s interior.The rock in the lithosphere is too cool for convection to continue.Heat moves through the lithosphere primarily by conduction.The lithosphere-asthenosphere boundary is 1300-1350oC, depending on depth.


Oceanic lithosphere is about 100 km thick.The geothermal gradient in oceanic lithosphere is 1300oC/100km, or 13oC/km.

Average continental lithosphere is 200 km. The average geothermal gradient in continental lithosphere is about 13500C/200 km, or 6.70C/km.

Earth’s Convection: Driven From the Top

Below the lithosphere, rock masses in the deeper mantle rise and fall according to differences in temperature and buoyancy( 浮力 ).

The densest lithosphere is most likely to sink back into the asthenosphere and the deeper mantle.

Ocean floor and the continents are slowly moving (up to 12 cm/yr).

Fig. 2.8

Plates and Mantle Convection

When continents split apart, a new ocean basin forms.

The Red Sea was formed this way 30 million years ago.

Subduction( 隱沒 ): the old lithosphere sinks beneath the edge of an adjacent plate.

Global Positioning System

In the 1960s, the U.S. Department of Defense established a network of satellites with orbits that could be used for reference in precisely determining location.

The Global Positioning System (GPS) detects small movements of the Earth’s surface.

Global Positioning System (2)

It is accurate within a few millimeters.

Two measurement methods: A GPS campaign: researchers establish a network

of fixed reference points on Earth’s surface, often attached to bedrock. The position is re-measured every few months or years.

Continuous GPS measurement: the receivers are attached permanently to monuments, and position is estimated at fixed intervals of a few seconds or minutes.

Fig. 2.9 A

Fig. 2.9

Fig. 2.9 c

Four Types Of Plate Margins And How They Move

The lithosphere currently consists of 12 large plates.

The seven largest plates are:North American Plate.

South American Plate.

African Plate.

Pacific Plate.

Eurasian Plate.

Australian-Indian Plate.

Antarctic Plate.

All are moving at speeds ranging from 1 to 12 cm a year.

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Plates have four kinds of boundaries or margins

Divergent margin (also called a spreading center): magma rises to form new oceanic crust between the two pieces of the original plate.Convergent margin/subduction zone: two plates move toward each other and one sinks beneath the other.Convergent margin/collision zone: two colliding continental plates create a mountain range.Transform fault margin: two plates slide past each other, grinding and abrading their edges.

Fig. 2.10

Seismology and Plate Margin

Earthquakes occur in portions of the lithosphere that are stiff and brittle.

Earthquakes usually occur on pre-existing fracture surfaces, or faults.

There are distinctive types of earthquakes that correlate nicely with motion at plate boundaries.

Three Types of Faults and Their Earthquakes

Strike-slip faults are vertical or near vertical fracture surfaces (at a plate boundary these are also known as transform faults).

Motion is entirely horizontal.Thrust faults are fracture surfaces that dip at an angle between the horizontal and the vertical (convergent motion within a volume of rock).

Motion is partly horizontal, partly vertical.Normal faults are fracture surfaces that also dip (divergent motion with and between bodies of rock).

Motion is partly horizontal, partly vertical, but opposite to the motion on a thrust fault.

Type I: Divergent Margin

Where two plates spread apart at a divergent boundary, hot asthenosphere rises to fill the gap.

As it ascends, the rock experiences a decrease in pressure and partially melts.

The molten rock is called magma.

Fig. 2.11

Fig. 2.12

Type I: Divergent Margin (2)

Midocean ridges occur in oceanic crust.

Found in every ocean.

Form a continuous chain that circles the globe.

Oceanic crust is about 8 km thick.

Fig. 2.13

Type II: Convergent Margin/Subduction Zone

Over 70 million years, oceanic lithosphere can drift 1500 to 3000 km from the spreading center.

As the plate cools, it grows denser.

The principle of isostasy demands that the plate subsides as it grows denser.

The process by which lithosphere sinks into the asthenosphere is called subduction.

Type II: Convergent Margin/Subduction Zone (2)

The margins along which plates are subducted are called subduction zones.

These are active continental margins.

The sinking slab warms, softens, and exchanges material with the surrounding mantle.


Under elevated temperature and pressure, the crust expels a number of chemical compounds.

Water (H2O).

Carbon dioxide (CO2).

Sulfur compounds.

A small addition of these volatile substances can lower the melting point of rock by several hundred degrees Celsius.


The hot mantle rock immediately above the sinking slab starts to melt.

Magma rises to the surface to form volcanoes.

Subduction zones are marked by an arc of volcanoes parallel to the edge of the plate.

Volcanoes At Subduction Zones

At a plate boundary, the plunging plate draws the seafloor down into an ocean trench, often 10 km deep or more.

If the overriding plate is oceanic lithosphere, volcanoes form a series of islands called a volcanic island arc.

Mariana Islands. Aleutian 阿留申 Islands.

Volcanoes At Subduction Zones (2)

If the overriding plate is continental lithosphere, a continental volcanic arc forms, while sediment washed from the continent tends to fill the offshore trench.

Cascade Range of the Pacific Northwest. The Andes of South America.

Volcanoes At Subduction Zones (3)

Chemical analyses of subduction-arc rocks disclose unusual concentrations of rare elements, such as boron, best explained by the expulsion of water and other volatile substances from the descending slab.

Most subduction-arc volcanoes occur roughly where earthquakes indicate that the top of the slab is 100 km deep.

Earthquakes in Subduction Zones

The largest and the deepest earthquakes occur in subduction zones.

The location of most earthquakes define the top surface of a slab as it slides into the mantle (the surface to as deep as 670 km).

Quakes deeper than 100 km are more likely associated with faults caused by stresses within the slab.

Type III: Convergent Margin/Collision Zone

Continental crust is not recycled into the mantle.

Continental crust is lighter (less dense) and thicker than oceanic crust.

When two fragments of continental lithosphere converge, the surface rocks crumple together to form a collision zone.

Type III: Convergent Margin/Collision Zone (2)

Collision zones that mark the closure of a former ocean form spectacular mountain ranges.

The Alps.

The Himalayas.

The Appalachians.

Fig. 2.16

Fig. 2.17

Type IV: Transform Fault Margin

Along a transform fault margin, two plates grind past each other in horizontal motion.

These margins involve strike-slip faults in the shallow lithosphere and often a broader shear zone deeper in the lithosphere.

Most transform fault occur underwater between oceanic plates.

Type IV: Transform Fault Margin (2)

Two of Earth’s most notorious and dangerous transform faults are on land.

The North Anatolian Fault in Turkey.

The San Andreas Fault in California.

Fig. 2.18

Topography of the Ocean Floor

Two main features:Midocean ridges.

Some 64,000 km in length. The spreading centers separate plates. The oceanic ridge with its central rift reaches sea

level and forms volcanic islands.– Iceland.

The oceanic trenches.

Hot Spots And Absolute Motion

During the nineteenth century, American geologist James Dwight Dana (1813-1895) observed that the age of extinct volcanoes in the Hawaiian Island chain increases as one gets farther away from the active volcanoes on the “big island.”The only active volcanoes are at the southeast end of the island chain, and the seamounts to the northwest are long extinct.Earthquakes occur only near the active volcanoes.

Hot Spots And Absolute Motion (2)

In the 1960’s, J. Tuzo Wilson proposed that a long-lived hot spot lies anchored deep in the mantle beneath Hawaii.A hot buoyant plume of mantle rock continually rises from the hot spot, partially melting to form magma at the bottom of the lithosphere—magma that feeds Hawaii’s active volcanoes.If the seafloor moves over the mantle plume, an active volcano could remain over the magma source only for about a million years.

Fig. 2.20

Fig. 2.21

Hot Spots And Absolute Motion (3)

As the plate moves, the old volcano would pass beyond the plume and become dormant.

A new volcano would sprout periodically through the plate above the hot spot, fed by plume magma.

The Hawaiian Islands connect with a chain of seamounts to the northwest.

These are dormant seafloor volcanoes that have sunk below the sea surface by erosion and isostasy.

The World’s Hot Spots

Several dozen hot spots have been identified worldwide.

Because hot spot volcanoes do not form tracks on the African Plate, geologists conclude that this plate must be very nearly stationary.

Hot spots transport roughly 10 percent of the total heat that escapes Earth.

The World’s Hot Spots (2)

Mantle plumes were probably more numerous 90-110 million years ago than today, because extinct seamount volcanoes of that age crowd together in the central Pacific.

Fig. 2.22

Figure 2.24 Largest volcano in the solar system (on Mars)

What Causes Plate Tectonics?

There is more agreement on how plate tectonics works than on why it works.

Mantle convection occurs in a variety of patterns, large-scale and small-scale.

Hotter rock is less viscous than cooler rock (critical to convective circulation).

What Causes Plate Tectonics? (2)

Hot, buoyant, low-viscosity material rises in narrow columns that resemble hot spot plumes.

Cooler, stiffer material from the surface sinks into the mantle in sheets (similar to subducting slabs).


Three forces seem likely to have a part in moving the lithosphere:

Ridge push: the young lithosphere sits atop a topographic high, where gravity causes it to slide down the gentle slopes of the ridge.Slab pull: at a subduction zone, as the cold, dense slab is free to sink into the mantle, it pulls the rest of the lithosphere into the oceanic trench behind it.


Friction: Slab friction drags the top, the bottom, and the

leading edge of descending lithosphere in the subduction zone.

Plate friction drags elsewhere at the base of the plate.

Figure 10.25

補充

Figure 10.26

Gutenberg discontinuity古氏 ; 地函與外地核的交界

Mohorovicic discontinuity莫氏 ; 地殼與地函的交界

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Global Tectonics