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The identity and significance of the high-latitude Early Ordovician Mediterranean brachiopod Province
The integration of palaeomagnetism, the geological record and mantle tomography in the location of ancient continents
Precisely locating the Ordovician equator in Laurentia
New global palaeogeographical reconstructions for the Early Palaeozoic and their generation
Abstract New palaeogeographical reconstructions are presented at 10 myr intervals from the Lower Cambrian at 540 Ma to the Lower Devonian at 400 Ma, showing continental crustal fragments and oceans (not lands and seas), with appropriate kinematic continuity between successive maps. The maps were chiefly generated by revised and selected palaeomagnetic data and revised Apparent Polar Wandering paths linked to present-day polygons from the main continents. These have been reinforced by analysis of the distributions of some fossils and sediments. Gondwana was the dominating supercontinent from its final assembly in the Latest Neoproterozoic at about 550 Ma until the Carboniferous, and covered much of the Southern Hemisphere. The Northern Hemisphere was largely occupied by the vast Panthalassic Ocean. The relative positions of the major continents and the latitudes and rotation histories of Gondwana, Baltica, Siberia and Laurentia (Laurussia from the mid-Silurian) are now well known. Although Laurentia was oriented in a similar direction to the present, Siberia was inverted throughout the Lower Palaeozoic, and Baltica too was initially inverted, but rotated through 120° between the Late Cambrian and Late Ordovician before collision with Laurentia in the mid-Silurian Caledonide Orogeny. Through reconstructions of the Caledonide and some other orogenies, the progressive history of the Iapetus Ocean between Laurentia and Baltica/Gondwana is well constrained. Less major continents whose positions are also well known include Avalonia (initially peri-Gondwanan but migrating in the Early Ordovician to join Baltica by the end of the Ordovician), Sibumasu (now considered an integral part of Gondwana) and Mongolia (adjacent to Siberia). A large number of other terranes are reviewed and plotted on the reconstructions with varying degrees of certainty. However, significant continents with less well constrained or controversial positions are South China, North China (Sinokorea), Annamia (Indochina) and Arctic Alaska–Chukotka. The European areas of France, Iberia and southern Italy, previously considered by some as a separate Armorican Terrane Assemblage, remained parts of core Gondwana until the opening of the Palaeotethys Ocean near the end of the Silurian, but it is uncertain whether Perunica (Bohemia) was one of that group or whether it left Gondwana during the Middle Ordovician.
A new Late Ordovician Hirnantia brachiopod Fauna from NW Turkey, its biostratigraphical relationships and palaeogeographical setting
The Palaeozoic palaeogeography of central Gondwana
Abstract Nine new palaeogeographical maps of central Gondwana are presented at intervals within the Palaeozoic from the Middle Cambrian at 510 Ma to the end of the Permian at 250 Ma. The area covered includes all of Africa, Madagascar, India and Arabia as well as adjacent regions, including parts of southern Europe, much of South America (including the Falkland Isles) and Antarctica. After final assembly in the Late Neoproterozoic the southern margin was largely passive throughout the Palaeozoic, apart from some local orogeny in the Cambrian in the final stages of the largely Neoproterozoic Pan-African Orogeny and during the Late Palaeozoic Gondwanide Orogeny. The northern peri-Gondwana margin was active during the Early Palaeozoic but the NW part became passive by the earliest Ordovician when the Rheic Ocean opened between Gondwana and Avalonia. This was eventually followed by the latest Silurian or Early Devonian opening of the Palaeotethys Ocean between Gondwana and Iberia, Armorica and associated terranes and, much later, the rifting and opening of the Neotethys Ocean near the close of the Permian. In the Late Carboniferous, Gondwana merged with Laurussia to form Pangea. That accretion took place outside the area to the NW, although the consequent orogenic activity extended to Morocco and Algeria. Most of the centre of Gondwana was land throughout the Palaeozoic but with extensive shelf seas over the craton margins, particularly the northern margin from the Cambrian to the Devonian on which the important north African and Arabian hydrocarbon source rocks were deposited in the Lower Silurian (with the chief reservoirs in the adjacent Upper Ordovician) and Upper Devonian. There were also substantial Upper Carboniferous and later non-marine lake basins in central and southern Africa in which the Karroo Supergroup was deposited. The South Pole was located within the area from the Early Palaeozoic to the Mid-Permian and central Gondwana was therefore greatly affected by two ice ages: the short but sharp Hirnantian glaciation at the end of the Ordovician and another lasting sporadically for more than 25 Ma during the later Carboniferous and Early Permian.
Correlation for the Lower Palaeozoic
Abstract In Lower Palaeozoic times, Gondwana was by far the largest tectonic entity, stretching from the South Pole to north of the Equator, and is termed a superterrane. We consider the northeastern sector of the Gondwanan and peri-Gondwanan margin, from Turkey through the Middle East, the north of the Indian subcontinent, southern China and SE Asia, to Australia and New Zealand. There was progressive tectonic activity along some of its margins during the period, with areas such as southeastern Australia undergoing enlargement through the accretion of island arcs as that part of Gondwana rotated. However, most of the area, from the Taurides of Turkey to at least east of India, represented a passive margin for the whole of the Lower Palaeozoic. Other adjacent areas, such as the Pontides of Turkey and Annamia (Indochina), were separate from the main Gondwanan craton as independent terranes. The quality and quantity of available data on Lower Palaeozoic rocks and faunas varies enormously over different parts of this substantial area, and there are few or no detailed palaeomagnetic data available for most of it. Some workers have considered the string of terranes from Armorica to the Malaysia Peninsula as having left Gondwana together in the late Cambrian as a Hun superterrane, leaving a widening Palaeotethys Ocean between it and Gondwana. However, we consider that the Palaeotethys opened no earlier than in late Silurian time (with Armorica and other terranes to its north), and that the Hun superterrane was not a cohesive unity. Other researchers vary in presenting many substantial Central Asian and Far Eastern terranes, including North China, South China, Tarim, Annamia and others, as integral parts of core Gondwana and not leaving it until Devonian and later times. We conclude that North China, Tarim and Annamia, among others, were probably not attached to core Gondwana in the Lower Palaeozoic, that South China was close to Gondwana (but not an integral part of it), and that Sibumasu was probably part of Gondwana. We try to reconcile the very varied published geological data and opinions, and present new palaeogeographical maps for that sector of Gondwana and surrounding areas for the Cambrian (500 Ma), Ordovician (480 Ma) and Silurian (425 Ma).
Caledonian tectonics
Abstract The Caledonian Orogeny lasted from the late Cambrian to the Devonian with the main collisional events occurring during Ordovician and Silurian times. Direct evidence of the extent of this orogenic event across central Europe is limited because of the lack of outcrops of this age. The Caledonian Orogeny, together with the subsequent Variscan and Alpine orogenies, is one of a succession of major tectonic events which have defined the geological evolution of Central Europe. Thus, the present configuration and condition of the lithosphere of central Europe is the result of superimposed periods of deformation (Fig. 7.1 ). Consequently, a wide range of investigative techniques needs to be employed to unravel these events in order to determine the properties of the various elements of the Caledonides and to elucidate the evolution of the Caledonian Orogeny. Additionally, evidence of the orogeny is deeply buried beneath thick successions of younger sediments, e.g. Dutch and North German Basin, or has been reworked extensively by later events, e.g. Belgium or to the SE of the Trans-European Suture Zone. The word ‘Caledonia’, the Latin name for northern Scotland, was used by Eduard Suess (1885-1909) not only to describe a geographic region but also to indicate an orogen he termed ‘Caledonisches Gebirge’. Furthermore, Suess was the first to put his definition into a tectonic context: ‘Die in der Kaledonischen Faltungsära gebildeten Gebirge treten vor allem in Irland, Wales, Schottland und im Westteil Skandinaviens in Erscheinung’. [The mountains built during the Caledonian folding era appear particularly in Ireland,
Late Ordovician global warming—The Boda event
Earth geography from 400 to 250 Ma: a palaeomagnetic, faunal and facies review
Quantifying paleogeography using biogeography: a test case for the Ordovician and Silurian of Avalonia based on brachiopods and trilobites
Key Lower Palaeozoic faunas from near the Trans-European Suture Zone
Abstract Following recognition of the Vendian to mid-Ordovician rotation of Baltica, with more than 55° of that rotation occurring in the Upper Cambrian and Lower Ordovician, the Tornquist Margin of Baltica must have faced northwards towards Laurentia and the Panthalassic Ocean, rather than, as now, southwestwards towards Gondwana (including Avalonia). Unequivocally Baltic endemic trilobite, brachiopod and other faunas are known from both the Cambrian and the Ordovician of the Holy Cross Mountains, Poland, and from both parts of them, i.e. the Małopolska Block and the Łysogóry Block. Whether or not these two blocks were united into a single terrane or were separate as two terranes is equivocal from the faunal evidence, and there is no faunal evidence of substantial strikeslip faulting of the blocks in relation to the main Baltic craton: they are perceived as having made up part of the margin of Baltica itself. However, both Holy Cross Mountain blocks were different and palaeogeographically separate from the Bruno-Silesian Block, whose continental origins are yet to be finally determined. The Ordovician clastic sediments at both Rügen, north Germany, and Pomerania, NW Poland, have yielded no macrofossils other than graptolites, but microfossils (acritarchs and chitinozoa) are interpreted as having been deposited at relatively high palaeolatitudes, i.e. at a higher palaeolatitude than Baltica, and may have been deposited in an ocean basin within the Tornquist Ocean between Baltica and Avalonia.