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The supercontinent cycle describes the quasi-periodic aggregration and dispersal of Earth's continental crust. There are varying opinions as to whether Earth's budget of continental crust is increasing, decreasing, or remaining about constant, but it is agreed that this inventory is constantly being reconfigured. One complete Supercontinent cycle is said to take 300 to 500 million years to occur.

Continental collision makes fewer and larger continents while rifting makes more and smaller continents. The last supercontinent, Pangaea, formed about 300 million years ago. The previous supercontinent, Pannotia, formed about 600 million years ago, and its dispersal formed the fragments that ultimately collided to form Pangaea. But beyond this the time span between supercontinents becomes more irregular. For example, the supercontinent before Gondwanaland, Rodinia, existed ~1.1 billion to ~750 million years ago - a mere 150 million years before Pannotia. The supercontinent before this was Columbia: ~1.8 to 1.5 billion years ago. And before this was Kenorland: ~2.7 to ~2.1 billion years ago. The first continents were Ur (existed ~3 billion years ago) and Vaalbara (~3.6 to ~2.8 billion years ago).

The hypothetical supercontinent cycle is, in some ways, the complement to the Wilson cycle. The latter is named after plate tectonics pioneer J. Tuzo Wilson and describes the periodic opening and closing of ocean basins. Because the oldest seafloor is only 170 million years old, whereas the oldest bit of continental crust goes back to 4 billion years or more, it makes sense to emphasize the much longer record of the planetary pulse that is recorded in the continents.

Contents 1 Effects on sea level 2 Relation to Global Tectonics 3 Relation to climate 4 Relation to evolution 5 References 6 External links

Effects on sea level

• It is known that, to a first-order, sea level is low when the continents are together and is high when they are apart. Thus sea level was low at the time of formation of Pangaea (Permian) and Pannotia (latest Neoproterozoic), rising rapidly to maxima during Ordovician and Cretaceous times, when the continents were dispersed.

• First-order sea level is controlled by the age of the seafloor. Oceanic crust lies at a depth (d) that is a simple function of its age (t):

d(t) = 2,500 + (350t^1/2)

where d is in meters and t is in millions of years, so that just-formed crust at the mid-ocean ridges lies at about 2,500 m depth, whereas 100 Ma-old seafloor lies at a depth of about 6,000 m.

Just as the water level in a bathtub is controlled by the size of the person in the bath, sea level is controlled by the depth of the seafloor (neglecting complications resulting from glacial ice and temperature effects). The relationship between seafloor depth and sea level can be expressed as follows:

The mass (M) of water on the earth is a constant = K₁, where

K₁ = M(seawater) + M(freshwater) + M(ice) + M(atm. water)

We can neglect M(freshwater) + M(atm. water)

K₁ = M(seawater) + M(ice)

Consider the ice-free world:

V(seawater) = K₁/(mean density of seawater)

This volume fills the ocean basins to a depth determined by A x d′, where A = area of the ocean basins and d′ = mean depth of the ocean basins. d′ is determined by the mean age of the seafloor.

A can change when continents rift (stretching the continents decreases A and raises sea level) or as a result of continental collision (compressing the continents leads to an increase A and lowers sea level). Increasing sea level will flood the continents, while decreasing sea level will expose continental shelves.

Because the continental shelf has a very low slope, a small increase in sea level will result in a large change in the percent of continents flooded.

If the world ocean on average is young, the seafloor will be relatively shallow, and sea level will be high: more of the continents are flooded. If the world ocean is on average old, seafloor will be relatively deep, and sea level will be low: more of the continents will be exposed.

There is thus a relatively simple relationship between the Supercontinent Cycle and the mean age of the seafloor.

• Supercontinent = lots of old seafloor = low sea level
• Dispersed continents = lots of young seafloor = high sea level

There will also be a climatic effect of the supercontinent cycle that will amplify this further:

• Supercontinent = continental climate dominant = continental glaciation likely = still lower sea level
• Dispersed continents = maritime climate dominant = continental glaciation unlikely = sea level is not lowered by this mechanism

Relation to Global Tectonics

There is a progression of tectonic regimes that accompany the supercontinent cycle:

During break-up of the supercontinent, rifting environments dominate. This is followed by passive margin environments, while seafloor spreading continues and the oceans grow. This in turn is followed by the development of collisional environments that become increasingly important with time. First collisions are between continents and island arcs, but lead ultimately to continent-continent collisions. This is the situation that was observed during the Paleozoic Supercontinent Cycle and is being observed for the Mesozoic-Cenozoic Supercontinent Cycle, still in progress.

Relation to climate

There are two types of global earth climates: Icehouse and Greenhouse. Icehouse is characterized by frequent continental glaciations and severe desert environments. We are now in the icehouse phase, moving towards Greenhouse. Greenhouse is characterized by warm climates. Both reflect the supercontinent cycle.

• Icehouse Climate
  • Continents moving together
  • Sea level low due to lack of seafloor production
  • Climate cooler, arid
  • Associated with Aragonite seas
  • Formation of Supercontinents

• Greenhouse Climate
  • Continents dispersed
  • Sea level high
  • High level of sea floor spreading
  • Relatively large amounts of CO₂ production at oceanic rifting zones
  • Climate warm and humid
  • Associated with Calcite seas

Periods of Icehouse Climate: Much of Neoproterozoic, Late Paleozoic, Late Cenozoic.

Periods of Greenhouse Climate: Early Paleozoic, Mesozoic-Early Cenozoic.

Relation to evolution

The principal mechanism for evolution is natural selection among diverse populations. As genetic drift occurs more frequently in small populations, diversity is an observed consequence of isolation. Less isolation, and thus less diversification, occurs when the continents are all together, producing both one continent and one ocean. In Latest Neoproterozoic to Early Paleozoic times, when the tremendous proliferation of diverse metazoa occurred, isolation of marine environments resulted from the breakup of Pannotia.

An arrangement of N-S continents and oceans leads to much more diversity and isolation than E-W oceans and continents. This forms zones that are separated by water or land and that merge into climatically different zones along communication routes to the north and south. Formation of similar tracts of continents and ocean basins, only oriented E-W would lead to much less isolation, diversification, and slower evolution. Through the Cenozoic, isolation has been maximized by an arrangement of N-S ocean basins and continents.

Diversity, as measured by the number of families, follows the supercontinent cycle very well.

References

• Gurnis, M., 1988, "Large-scale mantle convection and the aggregation and dispersal of supercontinents." Nature, 332:695-699
• Murphy, J. B., and R. D. Nance. 1992. "Supercontinents and the origin of mountain belts." Scientific American, 266(4):84-91
• Nance, R. D., T. R. Worsley and J. B. Moody. 1988. "The supercontinent cycle." Scientific American, 259(1):72-79

External links

• Plate reconstruction movies from UTIG 'PLATES' project

Wikipedia content modification information:

• This page was last modified on 10 October 2008, at 05:54.

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