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Sandbox 2

Climate
The Carboniferous climate was dominated by the LPIA, the most extensive and longest icehouse period of the Phanerozoic, which lasted from the Late Devonian to the Permian (365 Ma-253 Ma). (1,2) Temperatures began to drop during the late Devonian with a short-lived glaciation in the late Famennian through Devonian–Carboniferous boundary, (1) before the Early Tournaisian Warm Interval. (2) Following this, a reduction in atmospheric CO2 levels, caused by the increased burial of organic matter and widespread ocean anoxia led to climate cooling and glaciation across the south polar region. (Chen et al 39) During the Visean Warm Interval glaciers nearly vanished retreating to the proto-Andes in Bolivia and western Argentina and the Pan-African mountain ranges in southeastern Brazil and southwest Africa. (2)

The main phase of the LPIA (c. 335-290 Ma) began in the late Visean, as the climate cooled and atmospheric CO2 levels dropped. Its onset was accompanied by a global fall in sea level and widespread multimillion-year unconformities. (1) This main phase comprised of a series of discrete several million-year-long glacial periods during which ice expanded out from up to 30 ice centres that stretched across mid- to high-palaeolatitudes of Gondwana in eastern Australia, northwestern Argentina, southern Brazil, and central and Southern Africa. (1)

Isotope records indicate this drop in CO2 levels was triggered by tectonic factors with increased weathering of the growing Central Pangean Mountains and the influence of the mountains on precipitation and surface water flow. (Chen et al 39) Closure of the oceanic gateway between the Rheic and Tethys oceans in the early Bashkirian also contributed to climate cooling by changing ocean circulation and heat flow patterns. (10)

Warmer periods with reduced ice volume within the Bashkirian, the late Moscovian and the latest Kasimovian to mid-Gzhelian are inferred from the disappearance of glacial sediments, the appearance of deglaciation deposits and rises in sea levels. (1)

In the early Kasimovian there was short-lived (<1 myr) intense period of glaciation, with atmospheric CO2 concentration levels dropping as low as 180 ppm. (6a) This ended suddenly as a rapid increase in CO2 concentrations to c. 600 ppm resulted in a warmer climate. This rapid rise in CO2 may have been due to a peak in pyroclastic volcanism and/or a reduction in burial of terrestrial organic matter. (6a)

The LPIA peaked across the Carboniferous-Permian boundary. Widespread glacial deposits are found across South America, western and central Africa, Antarctica, Australia, Tasmania, the Arabian Peninsula, India, and the Cimmerian blocks, indicating trans-continental ice sheets across southern Gondwana that reached to sea-level. (1) In response to the uplift and erosion of the more mafic basement rocks of the Central Pangea Mountains at this time, CO2 levels dropped as low as 175 ppm and remained under 400 ppm for 10 Ma. (6a)

Temperatures
Temperatures across the Carboniferous reflect the phases of the LPIA. At the extremes, during the Permo-Carboniferous Glacial Maximum (299-293 Ma) the global average temperature (GAT) was c. 13 °C (55.4°F), the average temperature in the tropics 23.7 °C (74.7 °F) and in polar regions c. -23.1 °C (-9.6 °F), whilst during the Early Tournaisian Warm Interval (358-353 Ma) the GAT was c. 22.3 °C (72.1 °F), the tropics c. 30.0 °C (86 °F) and polar regions c. 1.5 °C (34.7 °F). Overall, for the Ice Age the GAT was c. 16.7 °C (62.1 °F), with tropical temperatures c. 26.0°C and polar temperatures c. -9.0 °C (15.8 °F). (2)

After the Early Tournaisian Warm Interval, the GAT cooled, warming briefly during the Visean Warm Interval (c. 18.8 °C (65.8 °F)), before dropping through the Pennsylvanian to c. 12.6 °C (54.7 °F) in the Mid-Gzhelian. During the Latest Gzhelian Thermal Excursion (300-299 Ma) GAT increased to c. 13.0 °C (55.4 °F), with the highest temperatures in the tropical regions (c. 25.4 °C (77.7 °F)) since the end of the Mississippian. However, after this brief interlude, temperatures dropped with the onset of the Permo-Carboniferous Glacial Maximum. (2)

Atmospheric oxygen levels
There are a variety of methods for reconstructing past atmospheric oxygen levels, including the charcoal record, halite gas inclusions, burial rates of organic carbon and pyrite, carbon isotopes of organic material, isotope mass balance and forward modelling. (3) Results from these different methods for the Carboniferous vary. For example, the increasing occurrence of charcoal produced by wildfires from the Late Devonian into the early Carboniferous indicates increasing oxygen levels, with calculations showing oxygen levels above 21% for much of the Carboniferous (4), whilst halite gas inclusions from the Visean give estimates at c. 15.3%, although with large uncertainties. (8,3) Combined results from the different methods, to give an estimate of atmospheric oxygen levels, show levels climbed rapidly from c. 20% at the start of the Carboniferous to c. 30% by its end. (3) The rise in atmospheric oxygen is attributed to the increased burial of organic matter in the widespread coal swamps. (12)

Effects of climate on sedimentation
The changing climate was reflected in regional-scale changes in sedimentation patterns. In the relatively warm waters of the Early to Middle Mississippian, carbonate production occurred to depth across the gently dipping continental slopes of Laurussia and North and South China (carbonate ramps architecture) (1) and evaporites formed around the coastal regions of Laurussia, Kazakhstania, and northern Gondwana. (12)

From the late Visean, the cooling climate restricted carbonate production to depths of less than c. 10 m forming carbonate shelves with flat-tops and steep sides. By the Moscovian, the waxing and waning of the ice sheets led to cyclothem deposition with mixed carbonate-siliciclastic sequences deposited on continental platforms and shelves. (1, 2)

Seasonal melting of glaciers resulted in near freezing waters around the margins of Gondwana. This is evidenced by the occurrence of glendonite (a pseudomorph of ikaite; a form of calcite deposited in glacial waters) in fine-grained, shallow marine sediments. (2)

The glacial grinding and erosion of siliciclastic rocks across Gondwana and the Central Pangaean Mountains produced vast amounts of silt-sized sediment. Redistributed by the wind, this formed widespread deposits of loess across equatorial Pangea. (14)

Effects of climate on biodiversity
The main phase of the LPIA was considered a crisis for marine biodiversity with the loss of many genera, followed by low biodiversity. However, recent studies of marine life suggest the rapid climate and environmental changes that accompanied the onset of the main glacial phase resulted in an adaptive radiation with a rapid increase in the number of species. (1)

The oscillating climate conditions also led to repeated restructuring of Laurasian tropical forests between wetlands and seasonally dry ecosystems, (10) and the appearance and diversification of tetrapods species. (7) There was a major restructuring of wetland forests during the Kasimovian glacial interval, with the loss of arborescent (tree-like) lycopisids and other wetland groups, and a general decline in biodiversity. These events are attributed to the drop in CO2 levels below 400 ppm. (1, 6a, 10). Although referred to as the Carboniferous rainforest collapse, this was a complex replacement of one type of rainforest by another, not a complete disappearance of rainforest vegetation. (7)

Across the Carboniferous–Permian boundary interval, a rapid drop in CO2 levels and increasingly arid conditions at low-latitudes led to a permanent shift to seasonally dry woodland vegetation (6a, 10) Tetrapods acquired new terrestrial adaptations and there was a radiation of dryland-adapted amniotes. (1)

Coal formation
Coal forms when organic matter builds up in waterlogged, anoxic environments (peat mires) and is then buried, compressing the peat into coal.(3) The majority of Earth's coal deposits were formed during the Late Carboniferous and Early Permian. The plants from which they formed contributed to changes in the Carboniferous Earth's atmosphere, and the coal itself fuelled the modern Industrial Revolution.(3)

During the Pennsylvanian, vast amounts of organic debris accumulated in the peat mires that formed across the low-lying, humid equatorial wetlands of the foreland basins of the Variscan-Alleghanian-Ouachita mountains in Laurussia, and around the margins of the North and South China continents.(3) During glacial periods, low sea levels exposed large areas of the continental shelves. Major river channels, up to several kilometres wide, stretched across these shelves feeding a network of smaller channels, lakes and peat mires.(1) These wetlands were then buried by sediment as sea-levels rose during interglacials. Continued crustal subsidence of the foreland basins and continental margins allowed this accumulation and burial of peat deposits to continue over millions of years resulting in the formation of thick and widespread coal formations. (3)

During the warm interglacials, smaller coal swamps with plants adapted to the temperate conditions, also formed on the Siberian craton and the western Australian region of Gondwana. (2)

There is ongoing debate as to why this peak in the formation of Earth's coal deposits occurred during the Carboniferous. The first theory, known as the delayed fungal evolution hypothesis, is that a delay between the development of trees with the wood fibre lignin and the subsequent evolution of lignin-degrading fungi gave a period of time where vast amounts of lignin-based organic material could accumulate. Genetic analysis of basidiomycete fungi, which have enzymes capable of breaking down lignin, supports this theory by suggesting this fungi evolved in the Permian. (24 and 25). However, significant Mesozoic and Cenozoic coal deposits formed after lignin-digesting fungi had become well established, and fungal degradation of lignin may have already evolved by the end of the Devonian, even if the specific enzymes used by basidiomycetes had not.(3) The second theory is that the geographical setting and climate of the Carboniferous were unique in Earth's history: the co-occurrence of the position of the continents across the humid equatorial zone, high biological productivity, and the low-lying, water-logged and slowly subsiding sedimentary basins that allowed the thick accumulation of peat were sufficient to account for the peak in coal formation.(3)



Geochemistry
As the continents assembled to form Pangea, the growth of the Variscan-Alleghanian-Ouachita mountains led to increased weathering and carbonate sedimentation on the ocean floor,(5) whilst the distribution of continents across the paleo-tropics meant vast areas of land were available for the spread of tropical rainforests.(1) Together these two factors significantly increased CO2 drawdown from the atmosphere, lowering global temperatures, increasing ocean pH and triggering the Late Paleozoic Ice Age.(5) The growth of the supercontinent also changed seafloor spreading rates and led to a decrease in the length and volume of mid-ocean ridge systems.(1)

Magnesium/calcium isotope ratios in seawater
During the Early Carboniferous, the Mg2+/Ca2+ ratio in seawater began to rise and by the mid-Mississippian aragonite seas had replaced calcite seas.(1) The concentration of calcium in seawater is largely controlled by ocean pH, and as this increased the calcium concentration was reduced. At the same time, the increase in weathering, increased the amount of magnesium entering the marine environment. As magnesium is removed from seawater and calcium added along mid-ocean ridges where seawater reacts with the newly formed lithosphere, the reduction in length of mid-ocean ridge systems increased the Mg2+/Ca2+ ratio further.(1) The Mg2+/Ca2+ ratio of the seas also affects the ability of organisms to biomineralize. The Carboniferous aragonite seas favoured those that secreted aragonite and the dominant reef builders of the time were aragonitic sponges and corals.(1)

Strontium isotopic composition of seawater
The strontium isotopic composition (87Sr/86Sr) of seawater represents a mix of strontium derived from continental weathering which is rich in 87Sr and from mantle sources e.g. mid-ocean ridges, which are relatively depleted in 87Sr. 87Sr/86Sr ratios above 0.7075 indicate continental weathering is the main source of 87Sr, whilst ratios below indicate mantle-derived sources are the principal contributor. (6)

87Sr/86Sr values varied through the Carboniferous, although they remained above 0.775, indicating continental weathering dominated as the source of 87Sr throughout. The 87Sr/86Sr during the Tournaisian was c. 0.70840, it decreased through the Visean to 0.70771 before increasing during the Serpukhovian to the lowermost Gzhelian where it plateaued at 0.70827, before decreasing again to 0.70814 at the Carboniferous-Permian boundary.(2) These variations reflect the changing influence of weathering and sediment supply to the oceans of the growing Variscan-Alleghanian-Ouachita mountain belt. By the Serpukhovian basement rocks, such as granite, had been uplifted and exposed to weathering. The decline towards the end of the Carboniferous is interpreted as a decrease in continental weathering due to the more arid conditions.(4)

Oxygen (δ18O) and carbon (δ13C) isotope ratios in seawater
Unlike Mg2+/Ca2+ and 87Sr/86Sr isotope ratios, which are consistent across the world's oceans at any one time, δ18O and δ13C preserved in the fossil record can be affected by regional factors.(2) Carboniferous δ18O and δ13C records show regional differences between the South China open-water setting and the epicontinental seas of Laurussia. These differences are due to variations in seawater salinity and evaporation between epicontinental seas relative to the more open waters.(2) However, large scale trends can still be determined. δ13C rose rapidly from c. 0 to 1‰ (parts per thousand) to c. 5 to 7‰ in the earliest Mississippian and remained high for the duration of the Late Paleozoic Ice Age (c. 3–6‰) into the earliest Permian.(2) Similarly from the Early Mississippian there was a long-term increase in δ18O values as the climate cooled.(3)

Both δ13C and δ18O records show significant global isotope changes (known as excursions) during the Carboniferous. (2) The mid-Tournaisian positive δ13C and δ18O excursions lasted between 6 and 10 million years and were also accompanied by c. 6‰ positive excursion in organic matter δ15N values, (3) a negative excursion in carbonate δ238U and a positive excursion in carbonate-associated sulphate δ34S. These changes in seawater geochemistry are interpreted as a decrease in atmospheric CO2 due to increased organic matter burial and widespread ocean anoxia triggering climate cooling and onset of glaciation. (2)

The Mississippian-Pennsylvanian boundary positive δ18O excursion occurred at the same time as global sea-level falls and widespread glacial deposits across southern Gondwana, indicating climate cooling and ice build-up. The rise in 87Sr/86Sr just before the δ18O excursion suggests climate cooling in this case was due to increased continental weathering of the growing Variscan-Alleghanian-Ouachita mountains and the influence of the orogeny on precipitation and surface water flow rather than increased burial of organic matter. δ13C values show more regional variation and it is unclear whether there is a positive δ13C excursion or a readjustment from previous lower values. (2)

During the earliest Kasimovian there was a short (<1myr), intense glacial period, which came to a sudden end as atmospheric CO2 concentrations rapidly rose.(3) The Kasimovian saw a steady increase in arid conditions across tropical regions and a major reduction in the extent of tropical rainforests, as shown by the widespread loss of coal deposits from this time. (4) The resulting reduction in productivity and burial of organic matter led to increasing atmospheric CO2 levels, which were recorded by a negative δ13C excursion and an accompanying, but smaller decrease in δ18O values. (3)

Etymology and history

The development of a Carboniferous chronostratigraphic timescale began in the late 18th century. The term "Carboniferous" was first used as an adjective by Irish geologist Richard Kirwan in 1799, and later used in a heading entitled "Coal-measures or Carboniferous Strata" by John Farey Sr. in 1811. Four units were originally ascribed to the Carboniferous, in ascending order, the Old Red Sandstone, Carboniferous Limestone, Millstone Grit and the Coal Measures. These four units were placed into a formalised Carboniferous unit by William Conybeare and William Phillips in 1822, and then into the Carboniferous System by Phillips in 1835. The Old Red Sandstone was later considered Devonian in age.(1)

The similarity in successions between the British Isles and Western Europe led to the development of a common European timescale with the Carboniferous System divided into the lower Dinantian, dominated by carbonate deposition and the upper Silesian with mainly siliciclastic deposition.(2) The Dinantian was divided into the Tournaisian and Viséan stages. The Silesian into the Namurian, Westphalian and Stephanian stages. The Tournaisian is the same length as the ICS stage, but the Viséan is longer, extending into the lower Serpukhovian.(5) North American geologists recognised a similar stratigraphy, but divided it into two systems rather than one. These are the lower carbonate-rich sequence of the Mississippian System and the upper siliciclastic and coal-rich sequence of the Pennsylvanian. The United States geological survey officially recognised these two systems in 1953. (1) In Russia, in the 1840’s British and Russian geologists divided the Carboniferous into the Lower, Middle and Upper series based on Russian sequences. In the 1890’s these became the Dinantian, Moscovian and Uralian stages. The Serpukivian was proposed as part of the Lower Carboniferous, and the Upper Carboniferous was divided into the Moscovian and Gzhelian. The Bashkirian was added in 1934. (5)

In 1975, the ICS formally ratified the Carboniferous System, with the Mississippian and Pennsylvanian subsystems from the North American timescale, the Tournaisian and Visean stages from the Western European and the Serpukhovian, Bashkirian, Moscovian, Kasimovian and Gzhelian from the Russian.(5) With the formal ratification of the Carboniferous System, the Dinantian, Silesian, Namurian, Westphalian and Stephanian became redundant terms, although the latter three are still in common use in Western Europe. (2)

Stratigraphy
The Carboniferous is divided into two subsystems; the Mississippian and Pennsylvanian. These are divided into three series and seven stages. The Tournaisian, Visean and Serpukhovian stages equate to the Lower, Middle and Upper series of the Mississippian respectively. The Bashkirian and Moscovian stages, the Lower and Middle Pennsylvanian and the Kasimovian and Gzhelian stages the Upper Pennsylvanian. (5) Only the boundaries of the Carboniferous System and three of the stage bases are defined by global stratotype sections and points (GSSPs) because of the complexity of the geology. (4 and 5)

Mississippian
The Mississippian was proposed by Alexander Winchell in 1870 named after the extensive exposure of Lower Carboniferous limestone in the upper Mississippi valley.(1) During the Mississippian, there was a marine connection between the Paleo-Tethys and Panthalassa through the Rheic Ocean resulting in the near worldwide distribution of marine faunas and so allowing widespread correlations using marine biostratigraphy (4 and 5). However, there are few Mississippian volcanic rocks and so obtaining radiometric dates is difficult.(4) The Tournaisian Stage is named after the Belgian city of Tournai. It was introduced in scientific literature by Belgian geologist André Dumont in 1832. The GSSP for the base of the Carboniferous System, Mississippian Subsystem and Tournaisian Stage is located at the La Serre section in Montagne Noire, southern France. It is defined by the first appearance of the conodont Siphonodella sulcata within the evolutionary lineage from Siphonodella praesulcata to Siphonodella sulcata. This was ratified by the ICS in 1990. However, in 2006 further study revealed the presence of Siphonodella sulcata below the boundary, and the presence of Siphonodella praesulcata and Siphonodella sulcata together above a local unconformity. This means the evolution of one species to the other, the definition of the boundary, is not seen at the La Serre site making precise correlation difficult. (5 and 6)

The Viséan Stage was introduced by André Dumont in 1832 and is named after the city of Visé, Liège Province, Belgium. In 1967, the base of the Visean was officially defined as the first black limestone in the Leffe facies at the Bastion Section in the Dinant Basin. These changes are now thought to be ecologically driven rather than due to evolutionary change, and so this has not been used as the location for the GSSP. Instead, the GSSP for the base of the Visean is located in Bed 83 of the sequence of dark grey limestones and shales at the Pengchong section, Guangxi, southern China. It is defined by the first appearance of the fusulinid Eoparastaffella simplex in the evolutionary lineage Eoparastaffella ovalis – Eoparastaffella simplex and was ratified in 2009. (5)

The Serpukhovian Stage was proposed in 1890 by Russian stratigrapher Sergei Nikitin. It is named after the city of Serpukhov, near Moscow. The Serpukhovian Stage currently lacks a defined GSSP. The Visean-Serpukhovian boundary coincides with a major period of glaciation. The resulting sea level fall and climatic changes led to the loss of connections between marine basins and endemism of marine fauna across the Russian margin. This means changes in biota are environmental rather than evolutionary making wider correlation difficult. (5) Work is underway in the Urals and Nashui, Guizhou Province, southwestern China for a suitable site for the GSSP with the proposed definition for the base of the Serpukhovian as the first appearance of conodont ''Lochriea ziegleri. (6)''

Pennsylvanian
The Pennsylvanian was proposed by J.J.Stevenson in 1888, named after the widespread coal-rich strata found across the state of Pennsylvania.(1) The closure of the Rheic Ocean and formation of Pangea during the Pennsylvanian, together with widespread glaciation across Gondwana led to major climate and sea level changes, which restricted marine fauna to particular geographic areas thereby reducing widespread biostratigraphic correlations. (4 and 5). Extensive volcanic events associated with the assembling of Pangea means more radiometric dating is possible relative to the Mississippian. (4)

The Bashkirian Stage was proposed by Russian stratigrapher Sofia Semikhatova in 1934. It was named after Bashkiria, the then Russian name of the republic of Bashkortostan in the southern Ural Mountains of Russia. The GSSP for the base of the the Pennsylvanian Subsystem and Bashkirian Stage is located at Arrow Canyon in Nevada, US and was ratified in 1996. It is defined by the first appearance of the conodont Declinognathodus noduliferus. Arrow Canyon lay in a shallow, tropical seaway which stretched from Southern California to Alaska. The boundary is within a cyclothem sequence of transgressive limestones and fine sandstones, and regressive mudstones and brecciated limestones. (5) The Moscovian Stage is named after shallow marine limestones and colourful clays found around Moscow, Russia. It was first introduced by Sergei Nikitin in 1890. The Moscovian currently lacks a defined GSSP. The fusulinid Aljutovella aljutovica can be used to define the base of the Moscovian across the northern and eastern margins of Pangea, however, it is restricted in geographic area, which mean it cannot be used for global correlations. (5) The first appearance of the conodonts Declinognathodus donetzianus or Idiognathoides postsulcatus have been proposed as a boundary marking species and potential sites in the Urals and Nashui, Guizhou Province, southwestern China are being considered. (6)

The Kasimovian is the first stage in the Upper Pennsylvanian. It is named after the Russian city of Kasimov, and was originally included as part of Nikitin's 1890 definition of the Moscovian. It was first recognised as a distinct unit by A.P. Ivanov in 1926, who named it the "Tiguliferina" Horizon after a type of brachiopod. The boundary covers of period of globally low sea level, which has resulted in disconformities within many sequences of this age. This has created difficulties in finding suitable marine fauna that can used to correlate boundaries worldwide.(5) The Kasimovian currently lacks a defined GSSP and potential sites in the southern Urals, southwest USA and Nashui, Guizhou Province, southwestern China are being considered. (6) The Gzhelian Stage is the second stage in the Upper Pennsylvanian. It is named after the Russian village of Gzhel, near Ramenskoye, not far from Moscow. The name and type locality were defined by Sergei Nikitin in 1890. The restricted geographic distribution of fauna is again a problem in defining the Kasimovian-Gzhelian boundary and the base of the Gzhelian currently lacks a defined GSSP. The first appearance of the fusulinid Rauserites rossicus and Rauserites stuckenbergi can be used in the Boreal Sea and Tethyan regions but not eastern Pangea or Panthalassa margins. (5) Potential sites in the Urals and Nashui, Guizhou Province, southwestern China for the GSSP are being considered.(6)

Carboniferous paleogeography
During the Carboniferous, there was an increased rate in tectonic plate movements as the supercontinent of Pangea assembled. The continents themselves formed a near circle around the opening Paleo-Tethys Ocean, with the massive Panthalassic Ocean beyond. The largest continent, Gondwana (modern day Africa, Arabia, South America, India, Madagascar, West Australia and East Antarctica), covered the south polar region. To its northwest was Laurussia (modern day North America, Greenland, Scandinavia, and much of Western Europe). These two continents slowly collided to form the core of Pangea. To the north of Laurussia lay Siberia and Amuria (central Mongolia). To the east of Siberia, Kazakhstania, North China and South China formed the northern margin of the Paleo-Tethys, with Annamia (Mainland Southeast Asia) laying to the south.(1)

alt text map of continents in the Late Carboniferous showing Laurussia and Gondwana combined to form Pangea. Siberia lays to the north, Amuria to its northeast. North and South China and Annamia form the northeastern margin of the Paleo-Tethys.

caption Position of the continents in the Late Carboniferous. Gondwana, Laurussia and Kazakhstania are already amalgamated as Pangea. Key: PA Panthalassa; S Siberia; AR Amuria; NC North China; SC South China; AN Annamia; PT Paleo-Tethys; red line approximate position of Variscan-Alleghanian-Ouachita Orogeny

An Early Carboniferous global marine transgression resulted in the widespread deposition of limestones in the warm, shallow seas of equatorial regions. (14) Sea levels then dropped as the Late Paleozoic Ice Age (LPIA) intensified in the Pennsylvanian, exposing large areas of continental shelf.(14) As glaciers waxed and waned repeated rises and falls in sea levels produced a distinctive pattern of terrestrial and marine sediments known as cyclothems. These consist of river channel and delta deposits with peat mires, followed by estuarine, coastal and offshore marine deposits as river deltas and wetlands built out across the continental shelves, only to be drowned as sea levels rose again.(15)

Variscan-Alleghanian-Ouachita Orogeny
Today the Variscan-Alleghanian-Ouachita Orogen stretches over 10,000 km from the present day Gulf of Mexico in the east to Turkey in the west (4). It formed between the Middle Devonian and Early Permian as a series of continental collisions between Laurussia, Gondwana and the Armorican Terrane Assemblage (much of modern day Central and Western Europe including Iberia) as the Rheic Ocean closed and Pangea formed. (2)

The Central Pangean Mountains were formed during the Variscan-Alleghanian-Ouachita Orogeny. Today their remains stretch over 10,000 km from the Gulf of Mexico in the east to Turkey in the west. The orogeny was caused by a series of continental collisions between Laurussia, Gondwana and the Armorican Terrane Assemblage (much of modern day Central and Western Europe including Iberia) as the Rheic Ocean closed and Pangea formed. This mountain building process began in the Middle Devonian and continued into the Early Permian.

The Armorican terranes rifted away from Gondwana during the Late Ordovician. As they drifted northwards the Rheic Ocean closed in front of them and they began to collide with southeastern Laurussia in the Middle Devonian.(2) The resulting Variscan Orogeny involved a complex series of oblique collisions with associated metamorphism, igneous activity, and large-scale deformation between these terranes and Laurussia, which continued into the Carboniferous.(2)

During the mid Carboniferous, the South American sector of Gondwana collided obliquely with Laurussia’s southern margin resulting in the Ouachita Orogeny.(2) The major strike-slip faulting that occurred between Laurussia and Gondwana extended eastwards into the Appalachian Mountains where early deformation in the Alleghanian Orogeny was predominantly strike-slip. As the West African sector of Gondwana collided with Laurussia, during the Late Pennsylvanian, deformation along the Alleghanian orogen became northwesterly-directed compression.(1 & 4)

Uralian Orogeny
The Ural Orogen is a north-south trending fold and thrust belt that forms the western edge of the Central Asian Orogenic Belt. (6 & 7) The Uralian Orogeny began in the Late Devonian and continued, with some hiatuses, into the Jurassic. From the Late Devonian to Early Carboniferous, the Magnitogorsk island arc, which lay between Kazakhstania and Laurussia in the Palaeo-Uralian Ocean, collided with the passive margin of northeastern Laurussia (Baltica craton). The suture zone between the former island arc complex and the continental margin formed the Main Uralian Fault, a major structure that runs for more than 2000 km along the orogen.(6) Accretion of the island arc was complete by the Tournaisian, but subduction of the Paleo-Ural Ocean between Kazakhstania and Laurussia continued until the Bashkirian when the ocean finally closed and continental collision began.(6)  Significant strike-slip movement along this zone indicates the collision was oblique. Deformation continued into the Permian and during the Late Carboniferous and Permian the region was extensively intruded by granites. (2, 6 & 7)

Laurussia
The Laurussian continent was formed by the collision between Laurentia, Baltica and Avalonia during the Devonian. At the beginning of the Carboniferous it lay at low latitude in the southern hemisphere and drifted north during the Carboniferous, crossing the equator during the mid-to-Late Carboniferous and reaching low latitudes in the northern hemisphere by the end of the Carboniferous.(1) The Variscan-Appalachian-Ouachita mountain ranges drew in moist air from the Paleo-Tethys resulting in heavy precipitation and a tropical wetland environment. Extensive coal deposits developed within the cyclothem sequences that dominated the Pennsylvanian sedimentary basins associated with the growing orogenic belt. (14 and 16)

Whilst the southern and southeastern margins of Laurussia were dominated by the Variscan-Alleghanian-Ouachita Orogeny and the northeasterly margin by the Uralian Orogeny, subduction of the Panthalassic oceanic plate along its western margin resulted in the the Antler Orogeny in the Late Devonian to early Mississippian. Further north along the margin, slab roll-back, beginning in the early Mississippian, led to the rifting of the Yukon-Tanana terrane and the opening of the Slide Mountain Ocean. Along the northern margin of Laurussia, orogenic collapse of the Late Devonian to early Mississippian Ellesmerian or Innuitian Orogeny led to the development of the Sverdrup Basin. (2)

Gondwana
Much of Gondwana lay in the southern polar region during the Carboniferous. As the plate moved, the South Pole drifted from southern Africa in the Early Carboniferous to East Antarctica by the end of the period. (1). Glacial deposits are widespread across Gondwana and indicate multiple ice centres and long distance movement of ice.(12)

The northern to northeastern margin of Gondwana (Northeast Africa, Arabia, India and northeastern West Australia) was a passive margin along the southern edge of the Paleo-Tethys with cyclothem deposition including, during more temperate intervals, coal swamps in Western Australia. (1). The Mexican terranes along the northwestern Gondwanan margin, were affected by the subduction of the Rheic Ocean.(2) However, they lay to west of the Ouachita Orogeny and were not impacted by continental collision, but became part of the active margin of the Pacific.(4) The Moroccan margin was affected by periods of widespread dextral strike-slip deformation, magmatism and metamorphism associated with the Variscan Orogeny. (1)

Towards the end of the Carboniferous, extension and rifting across the northern margin of Gondwana would led to the breaking away of the Cimmerian Terrane (parts of present-day Turkey, Iran, Afghanistan, Pakistan, Tibet, China, Myanmar, Thailand and Malaysia) during the early Permian and the opening of the Neo-Tethys Ocean. (2)

Along the southeastern and southern margin of Gondwana (eastern Australia and Antarctica), northward subduction of Panthalassa continued. Changes in the relative motion of the plates resulted in the Early Carboniferous Kanimblan Orogeny. Continental arc magmatism continued into the Late Carboniferous and extended round to connect with the developing proto-Andean subduction zone along the western South American margin of Gondwana. (1)

Siberia and Amuria
Shallow seas covered much of the Siberian craton in the Early Carboniferous. These retreated as sea levels fell in the Pennsylvanian and as the continent drifted north into more temperate zones extensive coal deposits formed in the Kuznetsk Basin. (16)

The northwest to eastern margins of Siberia were passive margins along the Mongol-Okhotsk Ocean on the far side of which lay Amuria. From the mid Carboniferous, subduction zones with associated magmatic arcs developed along both margins of the ocean.(2)

The southwestern margin of Siberia was the site of the long lasting and complex accretionary orogen. The Devonian to Early Carboniferous Siberian and South Chinese Altai accretionary complexes developed above an east-dipping subduction zone, whilst further south, the Zharma-Saur arc formed along the northeastern margin of Kazakhstania.(9) By the Late Carboniferous, all these complexes had accreted to the Siberian craton as shown by the intrusion of post-orogenic granites across the region. As Kazakhstania had already accreted to Laurussia, Siberia was effectively part of Pangea by 310Ma, although major transcurrent movements continued between it and Laurussia into the Permian.(2)

Central and East Asia
The Kazakhstanian microcontinent is composed of a series of Devonian and older accretionary complexes. It was strongly deformed during the Carboniferous as its western margin collided with Laurussia during the Uralian Orogen and its northeastern margin collided with Siberia. Continuing transcurrent motion between Laurussia and Siberia led the formerly elongate microcontinent to bend into an orocline.(2)

During the Carboniferous, the Tarim craton lay along the northwestern edge of North China. Subduction along the Kazakhstanian margin of the Turkestan Ocean resulted in collision between northern Tarim and Kazakhstania during the mid Carboniferous as the ocean closed. The South Tian Shan fold and thrust belt, which extends over 2000 km from Uzbekistan to Northwest China, is the remains of this accretionary complex and forms the suture between Kazakhstania and Tarim. (2 & 11). A continental magmatic arc above a south-dipping subduction zone lay along the northern North China margin, consuming the Paleoasian Ocean (1). Northward subduction of the Paleo-Tethys beneath the southern margins of North China and Tarim continued during the Carboniferous, with the South Qinling block accreted to North China during the mid to Late Carboniferous.(1 & 2)

No sediments are preserved from the Early Carboniferous in North China. However, bauxite deposits immediately above the regional mid Carboniferous unconformity indicate warm tropical conditions and are overlain by cyclothems including extensive coals.(1)

South China and Annamia (Mainland Southeast Asia) rifted from Gondwana during the Devonian.(2) During the Carboniferous, they were separated from each other and North China by the Paleoasian Ocean with the Paleo-Tethys to the southwest and Panthalassa to the northeast. Cyclothem sediments with coal and evaporites were deposited across the passive margins that surrounded both continents. Offshore eastern South China the proto-Japanese islands lay above a subduction zone consuming the Panthalassic Ocean.(1)

Cyclothems
A cyclothem is a succession of non-marine and marine sedimentary rocks, deposited during a single sedimentary cycle, with an erosional surface at its base. Whilst individual cyclothems are often only metres to a few tens of metres thick, cyclothem sequences can be many hundreds to thousands of metres thick, and contain tens to hundreds of individual cyclothems. (4) Cyclothems were deposited along continental shelves where the very gentle gradient of the shelves meant even small changes in sea level led to large advances or retreats of the sea.(2) Cyclothem lithologies vary from mudrock and carbonate-dominated to coarse clastic sediment-dominated sequences depending on the paleo-topography, climate and supply of sediments to the shelf.(1)

The main period of cyclothem deposition occurred during the Late Paleozoic Ice Age (LPIA) from the Pennsylvanian to Early Permian, when the waxing and waning of ice sheets led to rapid changes in eustatic sea level. (1) The growth of ice sheets led global sea levels to fall as water was lock away in glaciers. Falling sea levels exposed large tracts of the continental shelves across which river systems eroded channels and valleys and vegetation broke down the surface to form soils. The non-marine sediments deposited on this erosional surface form the base of the cyclothem.(1) As sea levels began to rise, the rivers flowed through increasingly water-logged landscapes of swamps and lakes. Peat mires developed in these wet and oxygen-poor conditions, leading to coal formation.(3) With continuing sea level rise, coastlines migrated landward and deltas, lagoons and esturaries developed; their sediments deposited over the peat mires. As fully marine conditions were established, limestones succeeded these marginal marine deposits. The limestones were in turn overlain by deep water black shales as maximum sea levels were reached. (2) Ideally, this sequence would be reversed as sea levels began to fall again, however, sea level falls tend to be protracted, whilst sea level rises are rapid - ice sheets grow slowly, but melt quickly. Therefore, the majority of a cyclothem sequence occurred during falling sea levels, when rates of erosion were high, meaning they were often periods of non-deposition. Erosion during sea level falls could also result in the full or partial removal of previous cyclothem sequences. Individual cyclothems are generally less than 10 m thick because the speed at which sea level rose gave only limited time for sediments to accumulate. (1)

During the Pennsylvanian, cyclothems were deposited in shallow, epicontinental seas across the tropical regions of Laurussia (present day western and central US, Europe, Russia and central Asia) and North and South China. (2) The rapid sea levels fluctuations they represent correlate with the glacial cycles of the Late Paleozoic Ice Age. The advance and retreat of ice sheets across Gondwana followed a 100 kyr Milankovitch cycle and so each cyclothem represents a cycle of sea level fall and rise over a 100 kyr period.(1)