OUR EARTH

EARTH – OUR HOME

Earth is the third planet from the Sun and the fifth largest:

Planet Profile

orbit: 149,600,000 km (1.00 AU) from Sun
diameter: 12,756.3 km
mass: 5.972e24 kg

History of Earth

Earth is the only planet whose English name does not derive from Greek/Roman mythology. The name derives from Old English and Germanic. There are, of course, hundreds of other names for the planet in other languages. In Roman Mythology, the goddess of the Earth was Tellus – the fertile soil (Greek: Gaia, terra mater – Mother Earth).

It was not until the time of Copernicus (the sixteenth century) that it was understood that the Earth is just another planet.

Mir and Earth's limbEarth, of course, can be studied without the aid of spacecraft. Nevertheless it was not until the twentieth century that we had maps of the entire planet. Pictures of the planet taken from space are of considerable importance; for example, they are an enormous help in weather prediction and especially in tracking and predicting hurricanes. And they are extraordinarily beautiful.

The Earth is divided into several layers which have distinct chemical and seismic properties (depths in km):

0- 40 Crust
40- 400 Upper mantle
400- 650 Transition region
650-2700 Lower mantle
2700-2890 D” layer
2890-5150 Outer core
5150-6378 Inner core

The crust varies considerably in thickness, it is thinner under the oceans, thicker under the continents. The inner core and crust are solid; the outer core and mantle layers are plastic or semi-fluid. The various layers are separated by discontinuities which are evident in seismic data; the best known of these is the Mohorovicic discontinuity between the crust and upper mantle.

Most of the mass of the Earth is in the mantle, most of the rest in the core; the part we inhabit is a tiny fraction of the whole (values below x10^24 kilograms):

atmosphere = 0.0000051
oceans = 0.0014
crust = 0.026
mantle = 4.043
outer core = 1.835
inner core = 0.09675

The core is probably composed mostly of iron (or nickel/iron) though it is possible that some lighter elements may be present, too. Temperatures at the center of the core may be as high as 7500 K, hotter than the surface of the Sun. The lower mantle is probably mostly silicon, magnesium and oxygen with some iron, calcium and aluminum. The upper mantle is mostly olivene and pyroxene (iron/magnesium silicates), calcium and aluminum. We know most of this only from seismic techniques; samples from the upper mantle arrive at the surface as lava from volcanoes but the majority of the Earth is inaccessible. The crust is primarily quartz (silicon dioxide) and other silicates like feldspar. Taken as a whole, the Earth’s chemical composition (by mass) is:Earth-South America

34.6% Iron
29.5% Oxygen
15.2% Silicon
12.7% Magnesium
2.4% Nickel
1.9% Sulfur
0.05% Titanium

The Earth is the densest major body in the solar system.

The other terrestrial planets probably have similar structures and compositions with some differences: theMoon has at most a small core; Mercury has an extra large core (relative to its diameter); the mantles ofMars and the Moon are much thicker; the Moon and Mercury may not have chemically distinct crusts; Earth may be the only one with distinct inner and outer cores. Note, however, that our knowledge of planetary interiors is mostly theoretical even for the Earth.

Unlike the other terrestrial planets, Earth’s crust is divided into several separate solid plates which float around independently on top of the hot mantle below. The theory that describes this is known as platetectonics. It is characterized by two major processes: spreading and subduction. Spreading occurs when two plates move away from each other and new crust is created by upwelling magma from below. Subduction occurs when two plates collide and the edge of one dives beneath the other and ends up being destroyed in the mantle. There is also transverse motion at some plate boundaries (i.e. the San Andreas Fault in California) and collisions between continental plates (i.e. India/Eurasia). There are (at present) eight major plates:

  • North American Plate – North America, western North Atlantic and GreenlandPlate boundaries
  • South American Plate – South America and western South Atlantic
  • Antarctic Plate – Antarctica and the “Southern Ocean”
  • Eurasian Plate – eastern North Atlantic, Europe and Asia except for India
  • African Plate – Africa, eastern South Atlantic and western Indian Ocean
  • Indian-Australian Plate – India, Australia, New Zealand and most of Indian Ocean
  • Nazca Plate – eastern Pacific Ocean adjacent to South America
  • Pacific Plate – most of the Pacific Ocean (and the southern coast of California!)

There are also twenty or more small plates such as the Arabian, Cocos, and Philippine Plates. Earthquakes are much more common at the plate boundaries. Plotting their locations makes it easy to see the plate boundaries.

The Earth’s surface is very young. In the relatively short (by astronomical standards) period of 500,000,000 years or so erosion and tectonic processes destroy and recreate most of the Earth’s surface and thereby eliminate almost all traces of earlier geologic surface history (such as impact craters). Thus the very early history of the Earth has mostly been erased. The Earth is 4.5 to 4.6 billion years old, but the oldest known rocks are about 4 billion years old and rocks older than 3 billion years are rare. The oldest fossils of living organisms are less than 3.9 billion years old. There is no record of the critical period when life was first getting started.

Strait of Gibraltar71 Percent of the Earth’s surface is covered with water. Earth is the only planet on which water can exist in liquid form on the surface (though there may be liquid ethane or methane on Titan’s surface and liquid water beneath the surface of Europa). Liquid water is, of course, essential for life as we know it. The heat capacity of the oceans is also very important in keeping the Earth’s temperature relatively stable. Liquid water is also responsible for most of the erosion and weathering of the Earth’s continents, a process unique in the solar system today (though it may have occurred on Mars in the past).

Earth's atmosphereThe Earth’s atmosphere is 77% nitrogen, 21% oxygen, with traces of argon, carbon dioxide and water. There was probably a very much larger amount of carbon dioxide in the Earth’s atmosphere when the Earth was first formed, but it has since been almost all incorporated into carbonate rocks and to a lesser extent dissolved into the oceans and consumed by living plants. Plate tectonics and biological processes now maintain a continual flow of carbon dioxide from the atmosphere to these various “sinks” and back again. The tiny amount of carbon dioxide resident in the atmosphere at any time is extremely important to the maintenance of the Earth’s surface temperature via the greenhouse effect. The greenhouse effect raises the average surface temperature about 35 degrees C above what it would otherwise be (from a frigid -21 C to a comfortable +14 C); without it the oceans would freeze and life as we know it would be impossible. (Water vapor is also an important greenhouse gas.)

Earth from Apollo 11The presence of free oxygen is quite remarkable from a chemical point of view. Oxygen is a very reactive gas and under “normal” circumstances would quickly combine with other elements. The oxygen in Earth’s atmosphere is produced and maintained by biological processes. Without life there would be no free oxygen.

The interaction of the Earth and the Moon slows the Earth’s rotation by about 2 milliseconds per century. Current research indicates that about 900 million years ago there were 481 18-hour days in a year.

Earth has a modest magnetic field produced by electric currents in the outer core. The interaction of thesolar wind, the Earth’s magnetic field and the Earth’s upper atmosphere causes the auroras (see theInterplanetary Medium). Irregularities in these factors cause the magnetic poles to move and even reverserelative to the surface; the geomagnetic north pole is currently located in northern Canada. (The “geomagnetic north pole” is the position on the Earth’s surface directly above the south pole of the Earth’s field.)

The Earth’s magnetic field and its interaction with the solar wind also produce the Van Allen radiation belts, a pair of doughnut shaped rings of ionized gas (or plasma) trapped in orbit around the Earth. The outer belt stretches from 19,000 km in altitude to 41,000 km; the inner belt lies between 13,000 km and 7,600 km in altitude.

Earth’s Satellite

Earth has only one natural satellite, the Moon. But

  • thousands of small artificial satellites have also been placed in orbit around the Earth.
  • Asteroids 3753 Cruithne and 2002 AA29 have complicated orbital relationships with the Earth; they’re not really moons, the term “companion” is being used. It is somewhat similar to the situation withSaturn’s moons Janus and Epimetheus.
  • Lilith doesn’t exist but it’s an interesting story.
           Distance  Radius    Mass
Satellite  (000 km)   (km)     (kg)
---------  --------  ------  -------
Moon       384         1738  7.35e22

More about Earth and the Moon

  • more Earth images and movies
  • the Blue Marble, very high resolution true color imagery
  • from NSSDC
  • U.S. Geological Survey
  • An image of Earth as seen from Mars taken by Mars Global Surveyor
  • pictures of Terrestrial Clouds from space (LANL)
  • text and pictures of Terrestrial Impact Craters (LANL)
  • pictures of Terrestrial and Hawaiian Volcanoes (LANL)
  • Volcano World
  • Electric Volcano
  • USA AVHRRGeomagnetism FAQ
  • more about the magnetic pole
  • A Beginner’s Guide to the Earth’s Magnetosphere
  • The Magnetosphere
  • Earth Viewer, an interactive map of the Earth
  • Earth As Seen From Space (images and astronaut quotes; by Calvin Hamilton of LANL)
  • Earth from Space, NASA images of Earth
  • Geography resources
  • why the sky is blue
  • Landsat images of the USA
  • AVHRR images
  • Encyclopedia of the Atmospheric Environment