In the Late Paleozoic, when the Cimmerian blocks were still located on the northern margin of Gondwana, they were far away from any active margins and orogenic belts, but they had been affected by
thermal subsidence since the Siluran opening of Paleo-Tethys.
Carboniferous to Permian ophiolites along suture zones in Tibet and north-eastern Iran indicate that the active margin of Paleo-Tethys was located here. It was slab-pull forces in the Paleo-Tethys that detached Cimmeria from Gondwana and opened the Neo-Tethys. The
mid-ocean ridge in the Paleo-Tethys subducted under Eurasia, as evidenced by Permian MORB (mid-ocean ridge basalt) in Iran. Slab roll-back in the Paleo-Tethys opened a series of
back-arc basins along the Eurasian margin and resulted in the collapse of the
Variscan cordillera. As the Paleo-Tethys subducted under the Eurasian southern margin, back-arc oceans formed from Austria to China. Some of these back-arcs closed during the Cimmerian orogeny (e.g. the Karakaya-Küre sequence of back-arc oceans in Turkey), others remained open (e.g. the Meliata-Maliac-Pindos back-arc oceans in the eastern Mediterranean) leading to the formation of younger back-arc oceans. During Early Jurassic, Cimmeria began to disintegrate behind the Paleo-Tethyan volcanic arc. This opened the northern branch in the Neo-Tethys—the Intra-Pontide, Izmh–Ankara, and the Inner Tauride oceans. The closure of the Paleo-Tethys in the Middle Jurassic reduced the Cimmerian archipelago in Anatolia. South of the Cimmerian blocks there were now two branches of the Neo-Tethys, a northern, larger and more complex, and a southern, more reduced. The Anatolide–Tauride continent separated them; the small Sakarya continent was located within the northern branch. The
Apulian continent was connected to the Anatolide–Tauride continent. In the Cretaceous, this basin pushed the Istanbul terrane (near today's Istanbul) southward in front of it, from the Odesa Shelf in the north-western Black Sea. In the Eocene, the terrane finally collided with Cimmeria thereby ending the extension in the western Black Sea. Contemporaneously, the East Black Sea Basin opened when the East Black Sea Block was rotated counter-clockwise towards Caucasus. In the late Cretaceous northwards intra-oceanic subduction within the Neotethys gave way to the obduction of ophiolitic nappes over the Arabian platform from Turkey to Oman region. North of this subduction zone, remnants of the Neotethys ocean started to subduct northwards and led to the collision of Tauride Block with the Arabian plate during post-Oligocene times. North of these systems, the Tauride block collided with the southern margin of Eurasia by the end of the Cretaceous. Convergence continued until the end of Oligocene. The Arabian-Eurasian collision in eastern Turkey during the Late Eocene closed the two basins. In southern Turkey the northward subduction of the Neo-tethys along the
Bitlis–
Zagros subduction zone resulted in magmatism in the Maden-Helete arc (south-eastern Turkey) during the Late Cretaceous-Eocene and back-arc magmatism in the Taurides. The Bitlis–Zagros subduction zone finally closed in the Miocene and throughout the Oligocene-Neogene and Quaternary volcanism became increasingly localised. In the Late Oligocene, slab roll-back in the
Hellenic Trench resulted in extension in the Aegean and western Turkey.
Caucasus The
Greater and
Lesser Caucasus have a complicated geological history involving the accretion of a series of terranes and microcontinents from the Late Precambrian to the
Jurassic within the Tethyan framework. These include the Greater Caucasian, Black Sea-Central Transcaucasian, Baiburt-Sevanian, and Iran-Afghanistan terranes and island arcs. In the Caucasus region remnants of the Paleo-Tethys suture can be found in the Dzirula Massif which outcrops Early Jurassic sequences in central
Georgia. It consists of Early Cambrian oceanic rocks and the possible remnants of a magmatic arc; their geometry suggests that suturing was followed by strike-slip faulting. Ophiolites also outcrop in the Khrami Massif in southern Georgia and another possible segment of the suture is present in the
Svanetia region. The suture is older east of the Caucasus (northern Iran–Turkmenistan) but younger both west of the Caucasus and further east in Afghanistan and the northern
Pamirs.
Sibumasu The easternmost part of Cimmeria, the
Sibumasu terrane, remained attached to north-western Australia until 295–290 Ma when it began to drift northward, as supported by paleomagnetic and biogeographic data. The
Qiangtang terrane was located west of Sibumasu and contiguous with it. Lower Permian layers in Sibumasu contain glacial-marine
diamictites and Gondwanan faunas and floras which then developed independently before Sibumasu docked with Cathaysia. Sibumasu's rapid northern journey is especially evident in the development of
brachiopods and
fusulinids. The
Baoshan terrane in western
Yunnan, China, forms the northern part of Sibumasu. It is separated from the
Burma block by the Gaoligong suture zone to the west, and from the South China and Indochina continents in the east by the Chongshan suture zone and Changning-Menglian belt. Like other parts of eastern Cimmeria, it was highly deformed by the intra-continental strike-slip faulting that followed the India-Asia collision. Paleomagnetic data indicate South China and Indochina moved from near equator to 20°N from the
early Permian to late Triassic. Baoshan, in contrast, moved from 42°S in the early Permian to 15°N in the late Triassic. These blocks and terranes occupied similar paleo-latitudes during late Triassic to Jurassic which indicates that they probably collided in the late Triassic. This is also supported by geological evidence: 200–230 Ma granite in
Lincang, near the Changning–Menglian suture, indicate a continent–continent collision occurred there in the late Triassic; pelagic sediments in the Changning–Menglian–Inthanon ophiolite belt (between Sibumasu and Indochina) ranges in age from middle Devonian to middle Triassic, while, in the Inthanon suture, in contrast, middle to late Triassic rocks are non-pelagic with radiolarian cherts and turbidic clastics indicating the two blocks had at least approached each other by that time; volcanic sequences from the
Lancangjiang igneous zone indicate a post-collisional setting had developed before the eruptions there around 210 Ma; and, the Sibumasu fauna developed from a non-marine peri-Gondwanan assemblage in the early Permian, to an endemic Sibumasu fauna in the
middle Permian, and to an Equatorial–Cathaysian in the late Permian. During the early and middle Palaeozoic, Cimmeria was located at an
Andean-style
active margin. Glacial deposits and
paleomagnetic data indicate that Qiangtang and Shan Thai–Malaya were still located far south adjacent to Gondwana during the Carboniferous. The equatorial fauna and flora of China indicate that it was separated from Gondwana during the Carboniferous. This proposed Late Triassic rifting of Lhasa has also been documented along the north-western shelf of Australia where the
West Burma and Woyla terranes eventually separated from Gondwana in the Late Jurassic. Today the
Bangong suture separates the Lhasa terrane from the Qiangtang terrane. ==Economic importance==