What makes Earth unique?

Soon after the Earth formed, unique processes occurred – division into metallic core, silicate mantle and crust – which, along with surface water, made it different from the other planets in our Solar System. The formation of the early mantle was important as it consisted primarily of ferromagnesium silicate minerals, some of which contained water as an essential component (e.g. amphibole group minerals). Water-bearing magmas (molten rock) from deep in the lower mantle then rose towards the surface (being liquid, they were lighter than the surrounding solid rock) and emerged as volcanic eruptions.

The Earth’s atmosphere and hydrosphere developed from the degassing (loss of gaseous elements such as carbon, hydrogen and oxygen) of the early-formed core and mantle during this volcanic activity. In the present, abundant gases are still released from the Earth during volcanic eruptions and these are mainly composed of water (77%), carbon dioxide (12%), sulfur dioxide (7%), and nitrogen (3%), with minor amounts of hydrogen, carbon monoxide, sulfur, chlorine and argon.

The Earth can be divided into two main parts.

• atmosphere: measured from the surface of the Earth upwards to 150 km (anything above this is called space)
• solid Earth: measured from the surface of the Earth downwards to the core

The atmosphere

The atmosphere makes up less than one millionth of the total mass of the Earth, and contains mainly nitrogen and oxygen (99% of the total) as gases. Other important components of the atmosphere are hydrogen, carbon dioxide, and inert gases such as argon and helium.

The Earth’s atmosphere and climate have changed since the Earth first formed more than four billion years ago. We know this from the geological record of the earliest known sedimentary rocks which could only have been deposited in water. Water boils above 100° C under normal atmospheric conditions. The presence of these early sedimentary rocks indicates that by four billion years ago, the surface temperature of the Earth must have cooled below 100° C. Also, some of these early sedimentary rocks are carbonate rocks (mainly dolomitic), indicating these rocks were formed in water that contained dissolved bicarbonate ions. The early atmosphere of the Earth must have contained more carbon dioxide than today’s atmosphere. Currently, the early atmosphere is understood to have consisted of nitrogen, carbon dioxide, carbon monoxide, water and hydrogen.

The atmosphere is divided (measured from the surface of the Earth) into:

• Troposphere (0 km – 13 km)
• Ozone Layer (13 km – 25 km)
• Stratosphere (25 km – 50 km)
• Mesosphere (50 km – 75 km)
• Thermosphere (75 km – 150 km)

The solid Earth

This can be divided into the:

• Biosphere (water, organic substances and skeletal matter) – solid and liquid – and includes all forms of life (e.g. plants and animals) and their products (e.g. skeletons) both on land and in the sea
• Hydrosphere (fresh and salt water, snow and ice) – mainly liquid, some solid – includes all forms of water
• Internal structure of the Earth, which includes:
  • Crust (normal silicate rocks such as granite and basalt) – solid
  • Mantle (ferromagnesium-rich silicate rocks) – solid
  • Core (iron-nickel alloy) – liquid upper part and solid lower part

Looking inside the Earth

The internal structure of the Earth consists of three main parts, the crust, mantle and core. The division between the crust and the mantle is called the Moho.

• The crust
• The Moho
• The mantle
• The core

The crust

The crust makes up only 0.5 % of the Earth’s total mass and can be subdivided into two main parts, continental and oceanic. Both differ in thickness, density and composition. Although oceanic crust covers approximately 61 % of the Earth’s surface, it only comprises some 30 % of the crustal mass, as the continental crust is much thicker.

Continental crust: from the surface of the Earth down to 30 km – 50 km. The exposed parts of the continental crust are less dense than oceanic crust (this is because oceanic crust contains minerals rich in heavier elements such as iron and magnesium). However, continental crust appears to be stratified (layered) and becomes denser with depth. It is largely composed of volcanic, sedimentary and granitic rocks, although the older areas are dominated by metamorphic rocks. The continental crust can be divided into:

1. Stable continental regions (e.g. Precambrian cratons, platforms of undeformed sediments on crystalline basements)
   Thickness: 35 km – 45 km
   Density: 2.69 gm/cm³ – 2.74 gm/cm³ for the upper crust and 3.0 gm/cm³ – 3.25 gm/cm³ for the lower crust.
   Composition
   • Upper Crust (sial): felsic igneous and metamorphic rocks. Average composition close to that of either a mafic granodiorite or quartz diorite.
   • Lower Crust (sima): anhydrous (no water) – quartz andesite or andesite; hydrous – amphibolite or diorite
2. Tectonically active regions (e.g. the Andes, Himalayas)
   Thickness: 55 km – 70 km
   Composition: varies from region to region but may consist of any of the following:
   1. mafic rocks
   2. amphibolites
   3. ultramafic, mafic and felsic-intermediate rocks

Oceanic crust: from the surface of the Earth down to 10 km – 12 km. The oceanic crust can be divided into:

1. Ocean basins: water depth exceeds 4 km, layered and very uniform and consists of three distinctive layers:
   • Layer 1: thickness of < 1 km; deep water sediments in various stages of lithification (turning into rock), commonly foraminiferal ooze, chert and mudstone.
   • Layer 2: thickness of 1.6 km – 2 km; basalts and dolerites with pillow lavas, dykes and sills (i.e. volcanic extrusive and intrusive rocks).
   • Layer 3: thickness of 3.0 km – 5.7 km; the main crustal layer; dolerite, gabbro and amphibolite (i.e. intrusive mafic rocks).
   • Layer 3B: thickness is variable but up to 3 km; not always present; metagabbros and pyroxenites (i.e. intrusive mafic and ultramafic rocks).
2. Mid-ocean ridges
   In mid-ocean ridges (such as the Mid-Atlantic Ridge), Layer 1 is absent; Layer 2 crops out on the surface and is thicker than normal; Layer 3 is thinner than normal and passes transitionally into the upper mantle.
3. Island arcs
   The structure beneath island arcs (such as the Indonesian Arc) is very complex and the composition of the crust in these regions is very heterogenous. The most common rocktypes in surface exposures are volcanic andesites (from explosive volcanoes) and deep-sea sediments.

The Moho

• a phase transition: The Moho may mark an isochemical phase transformation (i.e. change in mineralogy but not chemistry) from a gabbroic lower crust to an eclogitic upper mantle. However, this phase transformation appears to be a gradual process in oceanic and stable continental regions.
• a chemical discontinuity: The most widely accepted theory for the Moho is that it represents a chemical change from intermediate and mafic crustal rocks, to an ultramafic mantle.

The mantle

The mantle is thought to be primarily composed of ultrabasic rocks (rocks rich in magnesium and iron, and poor in silica; mostly peridotites). As seismic velocity change through the mantle, we can subdivide it into an upper mantle, transition zone, and lower mantle. There is also a zone in the upper mantle that we call the low velocity zone (located at depths of 70 km to 250 km) where S-wave speeds decrease rapidly to a minimum and then gradually increase again. We believe that most magmas (molten rock) are generated in this zone.

Upper mantle (measured from the base of the crust down to 400 km). 10 % of the Earth’s total mass.

• Density of 3.25 gm/cm³ to 3.40 gm/cm³
• Composition: Peridotite (e.g. olivine + pyroxene) along with plagioclase (< 30 km depth), spinel (30 km – 70 km depth) and garnet (> 70 km depth). In tectonically active regions, eclogite (amphibole + garnet) is a major component. Although it is thought that almost all basalts are derived from the upper mantle, experiments have shown that their compositions cannot be formed by the partial melting of peridotite alone. The upper mantle therefore is probably composed of two main zones: an upper peridotite zone and an underlying primitive mantle or pyrolite zone composed of pyroxene, olivine, and/or garnet and/or plagioclase, where basaltic magmas are generated.
• The pyrolite model: was first proposed by two Australian geoscientists, Green and Ringwood (1963), in order to explain the nature of the composition of the upper mantle. They recognised that most mantle xenoliths had previously undergone some partial melting in order to produce basaltic magmas. They suggested that a model composition of the undepleted upper mantle could be tested by experimental methods to determine the types of basaltic magmas that were produced. They made this by mixing three parts dunite (olivine-rich) with one part basalt (pyroxene and feldspar rich) and called this mixture pyrolite (pyroxene-olivine). Experimental melting studies on this mixture at differing values of pressure, temperature and volatile content has yielded the range of most known basalt compositions suggesting that it is a valid model for the composition of the upper mantle.

Transition zone (400 km – 1000 km below the Earth’s surface). 17 % of the Earth’s total mass.

• The top of the transition zone is marked by the phase transformation of normal olivine to a proto-spinel structure polymorph of olivine which is a higher pressure phase and is 9 % denser than normal olivine and by the phase transformation of normal pyroxene to a garnet-structure polymorph of pyroxene. Within the transition zone itself, there are a number of irregular seismic velocity changes including a major one at 680 km which is marked by the breakdown of olivine into its constituent oxide components of periclase (MgO) and stishovite (SiO₂). Also, garnet is broken-down to its component oxides from 680 km – 1000 km.

Lower mantle (1000 km – 2900 km below the Earth’s surface). 41 % of the Earth’s total mass.

• The lower mantle is a region of relatively low seismic velocity gradients. It most likely consists of mixed oxides of pyrolite composition but with an increased iron content.

The core

The core is marked as that point within the Earth where S-waves cannot penetrate. It is believed to be composed primarily of a nickel-iron alloy (along with abundant platinum-group elements), consisting of a liquid outer zone, and a solid inner zone. It is also marked by an abrupt increase in pressure.

• Outer core (2900 km – 5000 km below the Earth’s surface). 30 % of the Earth’s total mass.
• Inner core (5000 km – 6370 km below the Earth’s surface). 2 % of the Earth’s total mass.

Chemical composition of the Earth

The overall composition of the Earth is dominated by the elements iron (Fe), oxygen (O), silicon (Si), magnesium (Mg), nickel (Ni) and sulfur (S). This is because most of the mass of the Earth occurs within the mantle which is composed largely of the ferromagnesium silicate minerals olivine and pyroxenes. The core of the Earth is largely composed of iron and nickel. The crust of the Earth mainly comprises the minerals plagioclase, quartz and hornblende and is dominated by the elements oxygen, silicon, aluminium, iron, calcium, sodium, and potassium.

The overall composition of the Earth is very similar to that of meteorites, and because of this, it is thought that the Earth originally formed from Planetesimals composed largely of metallic iron and silicates.

P- and S-waves

• P-waves: Primary or Compressional Waves are the fastest type of wave and have velocities of 5 km/s at the top of the crust, 8 km/s at the top of the mantle, and 14 km/s at the bottom of the mantle. P-waves can travel through solids and liquids, so they can travel through the Earth’s core (the outer core is liquid).
• S-waves: Shear or Transverse waves that travel at slower speeds than P-waves. They can only travel through solids, so they do not travel through the Earth’s core.

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