Devonian

Disambiguation: "Devonian" is sometimes used to refer to the Southwestern Brythonic language, and the people of the county of Devon are sometimes referred to as "Devonians".

The Devonian is a geologic period of the Paleozoic era. It is named after Devon, England, where rocks from this period were first studied.

Important events

During the Devonian Period, which occurred in the Paleozoic era, the first fish evolved legs and started to walk on land as tetrapods, and the first arthropods like insects and spiders also started to colonize terrestrial habitats.

The first seed-bearing plants spread across dry land, forming huge forests. In the oceans, fish diversified into the first sharks, and the first lobe-finned and bony fish. The first ammonite mollusks appeared, and trilobites, the mollusc-like brachiopods, as well as great coral reefs were still common. The Late Devonian extinction severely affected marine life.

The paleogeography was dominated by the supercontinent of Gondwana to the south, the continent of Siberia to the north, and the early formation of the small supercontinent of Euramerica in the middle.

Naming

The period is named after Devon, a county in southwestern England, where Devonian outcrops are common. While the rock beds that define the start and end of the period are well identified, the exact dates are uncertain. According to the International Commission on Stratigraphy (Ogg, 2004), the Devonian extends from the end of the Silurian Period 416.0 ± 2.8 million years ago (Mya), to the beginning of the Carboniferous Period 359.2 ± 2.5 Mya (in North America, the beginning of the Mississippian subperiod of the Carboniferous) (ICS 2004).

The Devonian is also known as the Age of Fishes, but the term is out of favor. While fish underwent a major radiation it was only one of several major evolutionary landmarks during the period, and other lifeforms were more common.

The Devonian has also erroneously been characterized as a Greenhouse Age, due to sampling bias: most of the early Devonian-age discoveries came from the strata of western Europe and eastern North America, which at the time straddled the Equator as part of the supercontinent of Euramerica where fossil signatures of widespread reefs indicate tropical climates that were warm and moderately humid.

In nineteenth-century texts the Devonian has been called the Old Red Age, after the red and brown terrestrial deposits known in the United Kingdom as the "Old Red Sandstone" in which these early discoveries were found.

Devonian subdivisions

The Devonian is usually broken into Early, Middle, and Late subdivisions. The rocks corresponding to these epochs are referred to as belonging to the lower, middle, and upper parts of the Devonian System. The faunal stages from youngest to oldest are:

Late (most recent)

• Famennian/Chautauquan/Canadaway/Conneaut/Conneautan/Conewango/Conewangan
• Frasnian/Senecan/Sonyea/Sonyean/West Falls

Middle

• Cazenovia/Cazenovian
• Givetian/Erian/Senecan/Tioughniogan/Tioughnioga/Taghanic/Taghanican/Genesee/Geneseean
• Eifelian/Southwood

Early (oldest)

• Helderberg
• Emsian/Sawkill/Deer Park
• Pragian/Siegenian
• Lochkovian/Gedinnian

Devonian rocks are oil and gas producers in some areas.

Devonian palaeogeography

The Devonian period was a time of great tectonic activity, as Laurasia and Gondwanaland drew closer together.

The continent Euramerica (or Laurussia) was created in the early Devonian by the collision of Laurentia and Baltica, which rotated into the natural dry zone along the Tropic of Capricorn, which is formed as much in Paleozoic times as nowadays by the convergence of two great airmasses, the Hadley cell and the Ferrel cell. In these near-deserts, the Old Red Sandstone sedimentary beds formed, made red by the oxidized iron (hematite) characteristic of drought conditions.

Near the equator, Pangaea began to consolidate from the plates containing North America and Europe, further raising the northern Appalachian Mountains and forming the Caledonian Mountains in Great Britain and Scandinavia.

The west coast of Devonian North America, by contrast, was a passive margin with deep silty embayments, river deltas and estuaries, in today's Idaho and Nevada; an approaching volcanic island arc reached the steep slope of the continental shelf in Late Devonian times and began to uplift deep water deposits, a collision that was the prelude to the mountain-building episode of Mississippian times called the Antler orogeny [1].

The southern continents remained tied together in the supercontinent of Gondwana. The remainder of modern Eurasia lay in the Northern Hemisphere. Sea levels were high worldwide, and much of the land lay submerged under shallow seas, where tropical reef organisms lived.

The deep, enormous Panthalassa (the "universal ocean") covered the rest of the planet. Other minor oceans were Paleo-Tethys, Proto-Tethys, Rheic Ocean, and Ural Ocean (which was closed during the collision with Siberia and Baltica).

Devonian biota

Fossil trilobite Ductina vietnamica from the Devonian of China

Marine biota

Sea levels in the Devonian were generally high. Marine faunas continued to be dominated by bryozoa, diverse and abundant brachiopods and corals. Lily-like crinoids were abundant, and trilobites were still fairly common, but less diverse than in earlier periods. The ostracoderms were joined in the mid-Devonian by the first jawed fishes, the great armored placoderms, as well as the first sharks and ray-finned fish. The first shark, the Cladoselache, appeared in the oceans during the Devonian period. They became abundant and diverse. In the late Devonian the lobe-finned fish appeared, giving rise to the first tetrapods.

Reefs

A great barrier reef, now left high and dry in the Kimberley Basin of northwest Australia, once extended a thousand kilometers, fringing a Devonian continent. Reefs in general are built by various carbonate-secreting organisms that have the ability to erect wave-resistant frameworks close to sea level. The main contributors of the Devonian reefs were unlike modern reefs, which are constructed mainly by corals and calcareous algae. They were composed of calcareous algae and coral-like stromatoporoids, and tabulate and rugose corals, in that order of importance.

Terrestrial biota

By the Devonian Period, life was well underway in its colonization of the land. The bacterial and algal mats were joined early in the period by primitive plants that created the first recognizable soils and harbored some arthropods like mites, scorpions and myriapods. Early Devonian plants did not have roots or leaves like the plants most common today, and many had no vascular tissue at all. They probably spread largely by vegetative growth, and did not grow much more than a few centimeters tall.

By the Late Devonian, forests of small, primitive plants existed: lycophytes, sphenophytes, ferns, and progymnosperms had evolved. Most of these plants have true roots and leaves, and many were quite tall. The tree-like ancestral fern Archaeopteris, grew as a large tree with true wood. These are the oldest known trees of the world's first forests. By the end of the Devonian, the first seed-forming plants had appeared. This rapid appearance of so many plant groups and growth forms has been called the "Devonian Explosion". The primitive arthropods co-evolved with this diversified terrestrial vegetation structure. The evolving co-dependence of insects and seed-plants that characterizes a recognizably modern world had its genesis in the late Devonian. The development of soils and plant root systems probably led to changes in the speed and pattern of erosion and sediment deposition.

The 'greening' of the continents acted as a carbon dioxide sink, and atmospheric levels of this greenhouse gas may have dropped. This may have cooled the climate and led to a massive extinction event. see Late Devonian extinction.

Also in the Devonian, both vertebrates and arthropods were solidly established on the land.

Fungal life

While the marine fungi remained in the oceans and diversified into Nature's recyclers, land fungi were also recycling the land, decomposing both plants' and animals' dead bodies. Also, due to more terrestrial plants and animals appearance, fungi flourished.

Late Devonian extinction

A major extinction occurred at the boundary that marks the beginning of the last phase of the Devonian period, the Famennian faunal stage, (the Frasnian-Famennian boundary), about 364 million years ago, when all the fossil agnathan fishes, save for the psammosteid heterostracans, suddenly disappeared. A second strong pulse closed the Devonian period. The Late Devonian extinction was one of five major extinction events in the history of the Earth's biota, more drastic than the familiar extinction event that closed the Cretaceous.

The Devonian extinction crisis primarily affected the marine community, and selectively affected shallow warm-water organisms rather than cool-water organisms. The most important group to be affected by this extinction event were the reef-builders of the great Devonian reef-systems.

Amongst the severely affected marine groups were the brachiopods, trilobites, ammonites, conodonts, and acritarchs, as well as jawless fish, and all placoderms. Freshwater species, including our tetrapod ancestors, were less affected.

Reasons for the late Devonian extinctions are still speculative.

References

• Ogg, Jim; June, 2004, Overview of Global Boundary Stratotype Sections and Points (GSSP's) http://www.stratigraphy.org/gssp.htm Accessed April 30, 2006.

See also

• Geologic timescale
• Phacops rana: a Devonian trilobite.

External links

• UC Berkeley site introduces the Devonian.
• 'Devonian Times;' life and ecology.
• Devonian reef system in northwest Australia.
• International Commission on Stratigraphy (ICS). Geologic Time Scale 2004. Retrieved on Sept 19, 2005.
• Falls of the Ohio State Park USA, Indiana. One of the largest exposed Devonian fossil beds in the world.

Devonian period
Lower/Early Devonian	Middle Devonian	Upper/Late Devonian
Lochkovian | Pragian Emsian	Eifelian | Givetian	Frasnian | Famennian

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