What is Isostasy?
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| What is Isostasy? |
Isostasy is the rising or settling of a portion of the Earth’s lithosphere that occurs when weight is removed or added in order to maintain equilibrium between buoyancy forces that push the lithosphere upward and gravity forces that pull the lithosphere downward.
The principle of isostasy (or, simply, “isostasy”), which is
an application of Archimedes’ law of buoyancy to the Earth. Knowledge of
isostasy will help you to understand the elevation of mountain ranges and the
nature of gravity anomalies. To discuss isostasy, we must first review
Archimedes’ law.
Archimedes’ law states that when you place a
block of wood in a bathtub full of water, the block sinks until the mass of the
water displaced by the block is equal to the mass of the whole block
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The
concept of isostasy. (a) Blocks of wood
of different thicknesses float at different elevations when placed
in water. Therefore, the pressure at point A is the same as
the pressure at point B. (b) In the Earth, isostasy requires that
the mass of a column drilled down to the level of compensation
at A equals the mass of a column drilled at B, if isostatic equilibrium exists at both locations
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Now, imagine that you put two wood blocks of the same thickness but of different density in the water; this will be the case if one block is made of oak and the other is made of pine. The dense oak block floats lower than the less-dense pine block does. Note that, in the experiment, the pressure in the water at the base of the tub is the same regardless of which block floats above. Also, if you push down on or pull up on the surface of a block, it will no longer float at its proper depth.
If we make an analogy between the real Earth and our bathtub experiment, the lithosphere plays the role of the wooden blocks and the asthenosphere plays the role of the water. For a given thickness of lithosphere, the surface of more buoyant lithosphere floats higher than the surface of less buoyant lithosphere, if the lithosphere is free to float. Further, the pressure in the asthenosphere, at a depth well below the base of the lithosphere, is the same regardless of thickness and/or density of the lithosphere floating above (if the lithosphere is floating at the proper depth).
We call a depth in the asthenosphere at which the pressure is the same, regardless of location, a depth of compensation. With this image of floating lithosphere in mind, we can now state the principle of isostasy more formally as follows: When free to move vertically, lithosphere floats at an appropriate level in the asthenosphere so that the pressure at a depth of compensation in the asthenosphere well below the base of the lithosphere is the same. Where this condition is met, we say that the lithosphere is “isostatically compensated” or in “isostatic equilibrium.”
Another way to picture isostatic equilibrium is as
follows. If a location in the ocean lithosphere and a location in the
continental lithosphere are both isostatically compensated, then a column from
the Earth’s surface to the depth of compensation at the ocean location has the
same mass as a column of the same diameter to the same depth in the continental
location (Figure b).
Ocean basins exist because ocean crust is denser and thinner than continental crust, and thus ocean lithosphere sinks deeper into the asthenosphere than does continental lithosphere. Low-density water fills the space between the surface of the oceanic crust and the surface of the Earth.
Ocean basins exist because ocean crust is denser and thinner than continental crust, and thus ocean lithosphere sinks deeper into the asthenosphere than does continental lithosphere. Low-density water fills the space between the surface of the oceanic crust and the surface of the Earth.
Note that with isostasy in mind, we see that
changing the relative proportions of crust and mantle within the lithosphere
will change the depth to which the lithosphere sinks and thus will change the
elevation of the lithosphere’s surface. This happens because crustal rocks are
less dense than mantle rocks.
For example, if we increase the proportion of buoyant crust (by thickening the crust beneath a mountain range or by underplating magma to the base of crust), the surface of the lithosphere lies higher, and if we remove dense lithospheric mantle from the base of the plate, the plate rises. If the lithosphere doesn’t float at an appropriate depth, we say that the lithosphere is “uncompensated.” Uncompensated lithosphere may occur, for example, where a relatively buoyant piece of lithosphere lies embedded within a broad region of less buoyant lithosphere.
Because of its flexural rigidity, the surrounding lithosphere can hold the buoyant piece down at a level below the level that it would float to if unimpeded. The presence of uncompensated lithosphere causes gravity anomalies. Positive anomalies (gravitational pull is greater than expected) occur where there is excess mass, while negative anomalies (gravitational pull is less than expected) occur where there is too little mass.
For example, if we increase the proportion of buoyant crust (by thickening the crust beneath a mountain range or by underplating magma to the base of crust), the surface of the lithosphere lies higher, and if we remove dense lithospheric mantle from the base of the plate, the plate rises. If the lithosphere doesn’t float at an appropriate depth, we say that the lithosphere is “uncompensated.” Uncompensated lithosphere may occur, for example, where a relatively buoyant piece of lithosphere lies embedded within a broad region of less buoyant lithosphere.
Because of its flexural rigidity, the surrounding lithosphere can hold the buoyant piece down at a level below the level that it would float to if unimpeded. The presence of uncompensated lithosphere causes gravity anomalies. Positive anomalies (gravitational pull is greater than expected) occur where there is excess mass, while negative anomalies (gravitational pull is less than expected) occur where there is too little mass.
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