Faunal provinces

Ordovician faunas were strikingly provincial, much more so than those in the Silurian Period. The main control on the distribution of Ordovician faunas was temperature. The planktonic graptolites are commonly divided into the Pacific and Atlantic (or European) provinces. The Pacific Province corresponds to regions that were tropical during the Ordovician, such as North America, Siberia, Kazakhstan, and parts of China. The Atlantic Province is found in more-temperate regions of the Ordovician Period, including the British Isles, the Baltic region and Scandinavia, and northern Africa. Some modern regions, such as South America, straddled both of these provinces. Acritarchs follow a distribution similar to graptolites, with their faunas limited to tropical, polar, and intermediate regions in the Ordovician.

Conodont provinces include the North American Midcontinent and the North Atlantic provinces. The North American Midcontinent Province is also found in Scotland, Siberia, and temporarily in parts of the Baltic region and Scandinavia. The North Atlantic Province is known from the Baltic region and Scandinavia, the British Isles, and the margins of North America. Australian faunas bear similarities to both of these provinces yet have some distinctive elements, suggesting that they may represent another province.

Provinces have also been recognized within single continents for other groups. Late Ordovician corals from Laurentia have been divided into a Red River–Stony Mountain Province in the western United States and Canada and a Richmond Province, extending in a narrow belt from Ontario to Michigan to central Tennessee. In addition to all these temperature-controlled provinces, Ordovician faunas are known to change with water depth, nutrient levels, and sediment type. This regional isolation of many faunas contributed to the intense pace of the Ordovician radiation, but it has also made the global correlation of Ordovician rocks difficult.

Significant geologic events

A wide variety of rock types is found in the Ordovician System. Limestone and dolomite are the predominant rock types from the tropical epicontinental sea regions (that is, those that sit over continental shelves) in the Ordovician, such as Laurentia, Siberia, Kazakhstan, and South China. These limestones formed principally from the accumulation of calcareous skeletons of organisms, from carbonate mud, and from ooids (a type of seafloor sand) and peloids (small sand-sized grains formed from fecal matter, algae, and mud). Reefs are also commonly found in these limestone regions.

Ordovician evaporite deposits, such as anhydrite, are found in areas that were situated in arid belts near 30° N and 30° S. Anhydrite is known from the Early and Late Ordovician epochs of Laurentia and Kazakhstan.

Ordovician siliciclastic (made from broken parts of silica rocks) rocks can be divided into coarse-grained and fine-grained types. Relatively coarse-grained siliciclastic rocks such as sandstones and conglomerates tended to accumulate in high latitudes where significant carbonate accumulation was precluded and in low latitudes where orogenic uplift supplied abundant sediment. In North America, thick accumulations of coarse siliciclastic sediment can be found in the Appalachians. The Ordovician Taconic orogeny supplied voluminous amounts of sediment to the Queenston Delta, which spread from the Appalachians westward to Ontario and Ohio. Many of these sandstones are resistant to weathering and form the tops of ridges in the Ridge and Valley Province of the Appalachians. Additional thick sandstones are known from the Middle Ordovician Saint Peter Sandstone, which accumulated as a vast coastal sand dune system spread across much of North America. On other continents, thick successions of sandstones may be found in the Gondwana-associated regions of Antarctica, Australia, Great Britain, southern Europe, South America, and Africa. Coarse siliciclastic rocks also occur as glacial deposits in the late Late Ordovician of Africa and South America. These deposits consist of tilloids (gravity-driven sediments) and dropstones (rocks dropped into fine-grained sediments as they melted out of floating glacial ice).

Fine-grained siliciclastic rocks, represented by mudstones and shales, accumulated for the most part in deepwater settings of the Ordovician Period. As a result, thick accumulations of shale tend to occur around the margins of Ordovician continents and in the deepwater portions of epicontinental seas. Finely laminated black shales record deposition in anoxic (oxygen-depleted) water, whereas burrowed gray or red mudstones indicate oxygenated conditions. Bedded chert is sometimes associated with these basinal shales, as in China.

Volcanic ashes are known from many regions in the Ordovician Period, attesting to the widespread volcanism of the times. These ashes are commonly weathered to form K-bentonites (a type of clay useful in correlation because its particles are easily dated) that are interbedded with other rock types, such as limestone, shale, and sandstone. Other volcanic and igneous rocks are found principally near Ordovician subduction zones and back-arc basins (marine basins that form behind subduction zones), as in the British Isles, Kazakhstan, and China. Rock types include volcanic breccia, tuff, basalt, andesite, and rhyolite.

Economic significance of Ordovician deposits

Several types of Ordovician deposits are economically important. Petroleum and natural gas have been extracted from Middle and Upper Ordovician carbonates from the United States and Canada. Oil was first produced from a well that was drilled into Ordovician limestone in western Pennsylvania. Oil and natural gas continue to be produced from Middle and Upper Ordovician limestone and dolomite in the United States and Canada. Unusual oil-rich shales called kukersites are major sources of petroleum in Estonia. Limestone deposits in the Mississippi valley, central Tennessee, and the southern Appalachians are an important source of lead and zinc. Limestone itself is quarried in many places as a building stone, for use in roads, and for use in reducing sulfur emissions from coal-burning power plants. Phosphates have been mined for fertilizer from Ordovician limestones, particularly where weathering has concentrated the phosphate, as in central Tennessee. Ordovician sandstones, such as the Saint Peter Sandstone in the Midwestern United States, are important for glassmaking. Ordovician shales have been used to manufacture bricks. Black cephalopod-bearing limestones from Africa are widely sold as decorative pieces and tabletops.

Major subdivisions of the Ordovician System

The rocks that originated during the Ordovician Period constitute the Ordovician System. The Ordovician System is divided into seven stages—two each from the early and middle epochs and three from the late epoch. Of these, only three stages are named. The intense provincialism of Ordovician faunas has long hindered the establishment of a single global succession of stages and zones. Existing names and descriptions useful at regional levels are inconsistent and do not correlate well at the global level.

The International Commission on Stratigraphy (ICS) formed several working groups to define new stages based on a more accurate global correlation of stratigraphic and fossil markers. Ultimately, the period was divided into the Tremadocian (Stage 1), Floian (Stage 2), Dapingian (Stage 3), Darriwilian (Stage 4), Sandbian (Stage 5), Katian (Stage 6), and Hirnantian (Stage 7). Both the Tremadocian and Floian stages date to the Early Ordovician Epoch, which occurred between 485.4 million and 470 million years ago; the Dapingian and Darriwilian stages date to the Middle Ordovician Epoch, which occurred between 470 million and 458.4 million years ago; and the Sandbian, Katian, and Hirnantian stages date to the Late Ordovician Epoch, which occurred between 458.4 million and 443.8 million years ago.

Correlation of Ordovician strata

Correlation, or the demonstration of the age equivalence, of strata in the Ordovician System has traditionally relied on fossils. Shelly fossils, such as brachiopods (lamp shells) and trilobites, have proved most useful for correlation within individual continents because of their tendency to be endemic. Other shelly groups, including bryozoans (moss animals), crinoids, and corals, have also been used for correlation but to a lesser extent. The Cambrian-Ordovician boundary is marked by the first appearance of the conodont Iapetognathus fluctivagus and the trilobites Jujuyaspis borealis and Symphysurina bulbosa.

Graptolites (small, colonial, planktonic animals) and conodonts (toothlike remains of primitive chordates) are the most widely used organisms for the intercontinental correlation of Ordovician strata. Graptolites in particular are now used to define most of the new global Ordovician stage boundaries. Yet, even for this purpose, the effects of provinciality can limit their geographic ranges and thus their usefulness.

More recently, packages of rocks bounded by unconformities (interruptions in the deposition of sedimentary rock) have been used for correlation within continents. The field of sequence stratigraphy recognizes these units, termed depositional sequences. Many of these units may have formed from changes in global sea level and may ultimately be useful for global correlation.

Geochemical correlation of Ordovician rocks has also been successful. Broad correlations have been achieved with oxygen and carbon isotopes. Highly precise correlations of individual volcanic ash beds have been made using their major, minor, and trace element content.