These two halves of terranes were separated by Paleo-Tethys Ocean.

A new ocean was forming in its southern end, Paleo-Tethys Ocean.

It was an ocean predecessor of the later Paleo-Tethys Ocean.

East of the terranes that now form the Alps was the Paleo-Tethys Ocean.

Tectonic activities closed the Paleo-Tethys Ocean.

Paleo-Tethys Ocean started to shrink, while the new Tethys Ocean expanded.

About 250 million years ago, during the Triassic, a new ocean began forming in the southern end of the Paleo-Tethys Ocean.

The Paleo-Tethys Ocean was an ancient Paleozoic ocean.

A last remnant of Paleo-Tethys Ocean might be an oceanic crust under the Black Sea.

Two microcontinents, which are part of present-day China, lay in the eastern expanse of the Paleo-Tethys Ocean.

By the Late Triassic, all that was left of the Paleo-Tethys Ocean was a narrow seaway.

The Paleo-Tethys Ocean sat where the Indian Ocean and Southern Asia are now located.

It opened farther westward in the mid-Triassic, at the expense of the shrinking Paleo-Tethys Ocean, an ocean that existed during the Paleozoic.

The rocks were formed at a passive margin of the Paleo-Tethys Ocean, when the Austroalpine terrain was part of the micro-continent Avalonia.

Tectonic activities are active on eastern Laurasia as the Cimmerian plate continues to collide with Laurasia's southern coast, completely closing the Paleo-Tethys Ocean.

Late Carboniferous Map - at PaleoMap Project; a good picture of Paleo-Tethys Ocean before the Cimmerian Plate moves northward.

The ocean closed when the North China craton collided with Siberia-Kazakstania continent in the Carboniferous, while the Paleo-Tethys Ocean expanded.

At the end of the Permian a connection with the Paleo-Tethys Ocean to the south was formed in present day southeast Poland, causing sea water to flow in periodically.

As the Tethys Ocean widened, it pushed Cimmeria and the floor of the Paleo-Tethys Ocean northward towards Laurasia, the northeastern arm of Pangaea.

The Paleo-Tethys Ocean, mentioned above, existed from the Silurian (440 Ma) through the Jurassic periods, between the Hunic terranes and Gondwana (later the Cimmerian terranes).

The mountain range formed at the northern edges of the Cimmerian Plate during its collision, in the Late Triassic, with Siberia, which resulted in the closing of the Paleo-Tethys Ocean.

Over the next 60 million years, that piece of shelf, known as Cimmeria, traveled north, pushing the floor of the Paleo-Tethys Ocean under the eastern end of Northern Pangaea (Laurasia).

The collision of Sibumasu terranes and Indochina terranes during 200mya Late Triassic resulted in the closure of the Paleo-Tethys Ocean and formation of the modern Titiwangsa Mountain belts.

By Early Permian time, the Cimmerian plate split from Gondwana and headed towards Laurasia, thus closing the Paleo-Tethys Ocean, but forming a new ocean, the Tethys Ocean, in its southern end.

By late Silurian time, North and South China split from Gondwana and started to head northward, shrinking the Proto-Tethys Ocean in their path and opening the new Paleo-Tethys Ocean to their south.