The beginnings of the Plate Tectonic Theory began with a German Meteorologist
by the name of Alfred Wegener. He put forth in 1915 a radical proposal
that continents had drifted about the face of the Earth. His proposal
became known as Continental Drift. He hypothesized
that prior to 200 Ma. all of the continental land masses were welded into
a single "super continent" which he called Pangea (Greek meaning "all earth").
This super continent began to break up about 200 million years ago into
smaller continents which then "drifted" to their current positions.
He and a small group of others collected substantial evidence to support
1) fit of South America and Africa
2) ancient climatic similarities, esp. polar glaciation
3) similar rock structures on either side of the Atlantic
4) fossil evidence
Wegener's book was translated into English in 1924 and was greeted with nothing short of hostile criticism by the North American Scientific Community. The theory of Continental drift was largely rejected because Wegener was unable to provide a viable mechanism to drive the moving continents.
During WWII, the U.S. Navy's search for German submarines in the Atlantic Ocean, using SONAR and sensitive magnetometers, produced a wealth of data that would ultimately lead to conclusive proof of the dynamic nature of the lithosphere. Based on these data, the concept of Sea Floor Spreading became widely accepted, and this concept -- one describing the formation of new oceanic crust at mid-ocean ridges and the subsequent spreading of that crust -- led to the development of the theory of Plate Tectonics.
Before examining the theory of Plate Tectonics, it is
necessary to learn about the generation and transfer of heat within the
interior, and how we measure this flow of heat.
Heat that originally produced prior to, and during the Iron Catastrophe is concentrated in the deep interior (lower mantle and core). For the past 4.6Ga, this heat has been slowly transferred from the deep interior to the surface as the Earth cools. Owing to the fact that rocks are not good heat conductors, the primary mode of heat transfer is by convection of the hot, plastic asthenosphere.
The transfer of heat from the interior to the surface is measured as heat flow. On continents, heat flow is usually measured in deep drill cores. Temperatures are measured going down the drill hole and establish a temperature gradient. Rocks that form the drill core are them measured for the thermal conductivity. Knowing the temperature variation with depth and the conductivity, we can calculate the heat flow, usually expressed in units of micro-calories/cm2 /sec.
It turns out that
it is possible to separate the effects of radiogenic heat production in
the crust from flow of heat coming from the mantle. The figure to
the left illustrates how this can be done (for more details see p. 371
of your textbook). For a given section of crust, heat flow from the
mantle is a constant, whereas heat produced by radioactive decay depends
on the composition of the crust (i.e., how much radioactive isotopes are
present. If we measure the heat flow, and can determine how much
heat is produced in the underlying crustal rocks (by knowing their radioactive-isotope
content), a linear relationship results. THe constant in the linear
equation is the heat flowing from the mantle into the base of the crust.
Heat flow, and calculated geothermal gradients vary greatly from place to place. The figure to the left illustrates the calculated geothermal gradients for the eastern U.S. and the Basin and Range Province in the western U.S. Note that at 35 km depth (the "normal" depth of the MOHO beneath continents, the Basin and Range is roughly twice as hot as is the eastern part of the continent. The "hot" character of the Basin and Range Province coincides with its geologic and tectonic activity ( it is young and hot). Furthermore the high heat flow values cannot be entirely explained by heat production in the crust. The mantle beneath this region must also be hotter than normal. In contrast the eastern U.S. consists of old and cold crust, lithosphere and asthenosphere.
Heat flow in the ocean basins is also highly variable. The highest values correspond to the mid-ocean ridges. Heat flow decreases away from the mid-ocean ridges and is at a minimum over the convergent plate boundaries, deep ocean trenches or subduction zones. In general lithosphere is hot where the underlying asthenosphere is hot, and cold here it is cold. This observation strongly supports the concept that plate tectonics is largely driven by convection within the asthenosphere. Sites characterized by upwelling of hot asthenosphere (the rising limbs of convection cells) have high heat flow (e.g., mid-ocean ridges). In contrast areas where the convection cells turn and sink back into the deep interior are cold (e.g., subduction zones).
At present, the Earth's lithosphere can be divided into 14 - 16 recognized plates, each moving at different velocities and in relatively different motions. The 14 major plates are shown in the following figure:
The figure above, not only identifies the individual plates but also gives their realtive movement and velocities (in cm/yr of either convergence or divergence).
Lithospheric plates are defiend on the basis of their boundaries. These boundaries are large-scale major fault boundaries. As such they are easily recognized by the fact that many earthquakes occur along the boundaries. The boundaries associated with mid-ocean ridges (divergent boundaries) are characterized by frequent, shallow and low-magnitude earthquakes. Convergent boundaries (typically subduction zones) are characterized by earthquakes that are shallow near the intersection of the boundary with the surface, but increase with depth in the direction of convergence. This increase in depth of earthquakes defines the dipping slab of lithosphere descending into the mantle (the Benioff zone).
Plate boundaries are classified as follows (Please refer to your text and lecture notes for further details of each type of boundary):
I. Divergent Boundaries
Our current understanding of plate motions (directions) and velocities comes from a combination of two sources of data:
Use of paleomagnetism to determine plate motion can be illustrated with reference to magnetic inclination. The figure to the left (fig. 19-5 in Press and Siever) shows the magnetic field associated with the Earth and the directions that a compass needle will point at various latitudes. Note that at either magnetic pole the needle will point toward the center of the earth; at the equator it will be horizontal; and at all other latitudes it will be inclined with the amount of inclination being determined by the latitude.
Igneous rocks are ideal candidates for determining the state of the Earth's magnetic field at the time the rock crystallized and cooled. Igneous rocks contain minor quantities of minerals that are magnetic. When igneous rocks (e.g., lava flows) crystallize and coole below a certain temperature (the Curie temperature), the magnetic minerals will align their magnetic moments with the magnetic field of the Earth at that time. Oriented specimens of igneous rocks can be collected in the field and the magnetic properties of the rocks can be analyzed in the lab. The resultant data include the magnetic inclination of the rock, and hence the geographic latitude at the time the rock formed. If we can also determine the age of formation, then we know the latitude of the rock when it formed.
A simple example
is given in the figure to the left. Consider a volcanic island located
on a plate moving from south to north. Samples collected from 4 different
, progressively younger, lava flows on the volcano can be both dated and
their paleomagnetic inclinations determined. In this case, the oldest
flows (1&2) erupted in the southern hemisphere; flow 3 erupted at the
equator and flow 4 erupted in the northern hemisphere. Precise inclination
data combined with ages of eruption allow reconstruction of the movement
of this island (and the lithospheric plate it is sitting on) with time.
From these data, we can reconstruct the relative movement of the plate
with time (relative to the Earth's magnetic poles).
2. The tracks of Hot Spots
Hot spots are considered to represent the surface manifestation of plumes of hot material that rise from very deep within the mantle, drill through the lithosphere and emerge as volcanic centers on either the sea floor or on continental crust. The source for the plumes is apparently fixed in the lower mantle, and consequently is not affected by movement of lithospheric plates. As a result, a hot spot produces a linear trail of extinct, progressive older volcanoes as a plate moves over it.
The best example of a hot spot track is the chain of oceanic volcanic islands that include the Hawaiian islands and, extending to the NW the Emperior Seamount chain. This spectacular example is shown below:
Note the prgressively decreasing age of volcanic rocks going from the NW to the SE in both the Hawaiian Islands proper and their counterparts to the NW, including Midway and extending all thte way to the Aleutian Islands. This entire chain of volcanic islands formed as the Pacific Plate passed over a hot spot. The age of volcanic rocks and their relative position provides a recording of Pacific Plate movement and velocity for the past 60Ma. It is also very apparent that the motion of hte Pacific Plate made an abrupt change at approximately 40Ma (corresponding to the "kink" in the linear trend of volcanoes).
Tracks of hot Spots have also been identified on the continents. The best known (at least to me), is the Yellowstone Hot Spot, which marks the path of North America over a hot spot currently located beneath Yellowstone National Park. Relative to this hot spot, the North American Plate has moved to the SW, producing a linear trend of volcanism defining the Snake River Plain.
Hot spots and deep mantle plumes are currently hot topics (pun intended) for research in geology, and this research promises to give us a better understanding of the workings of not only plate tectonics, but also of the deep mantle.