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littoral deposits ; and there can be no doubt that the last mentioned 
reefs both inside and outside the “graben” all belong to one and 
the same continuous formation, the connection of which has only 
been interrupted by later erosion. 
During and just after the formation of these coralreefs a great 
portion of Middle-Timor must have been covered by a sea full of 
coral-islands and reefs. The higher mountain-groups ,Moetis, Lakaän, 
Mandeo etc.) emerged as islands from this sea, and the conglome- 
rates, formed simultaneously with and posterior to the coralreefs, 
prove that the islands must have been steep and high and that the 
running water must have transported a considerable amount of debris 
from them towards the surrounding sea. 
It may be accepted that the majority of the big coralreefs were 
thus formed in late plioeene or early pleistocene times as they overlie 
and clearly therefore indicate a younger age than the marls with 
plioeene shells. 
Further, as these reefs were already formed, a general upheaval 
of the island of Timor took place whieb possibly still continues. 
This upheaval, however, was not equally strong everywhere, conse- 
quently the elevated coralreefs are no longer found in a horizontal 
position but feebly sloping. 
It appears that the upheaval of the central portion ee the island 
has been from the beginning somewhat stronger than that of the 
southern and northern coastal regions. 
In fact the reefs of the Diroen-ridge south of the Lakaän near the 
central axis of the island occur now at an altitude of 1283 Meters, 
about 680 Meters higher than those on the hills of the north coast 
at Babilo. The big reef also of the Gempol-cliff in the central portion 
of the island not far from Kapan has an altitude of 1250 Meters 
above sealevel, whereas in the southern mountainranges near Niki- 
Niki the highest altitude at which coralreefs are found is only 
750 Meters. 
Moreover, the upheaval of the land has been stronger at the edges 
of the basins (‘“‘graben’’) than in the basins themselves. Consequently 
the coralreefs which rest on the pliocene strata in the ‘graben’ are 
no longer found in their original horizontal plane of deposition, but 
assume a feebly basin- or trough-shaped position and are besides 
split up into blocks of slightly different altitudes. It may be that this 
latter circumstance is caused by compression and the squeezing out 
of the soft and more or less plastic plivcene strata underlying the 
heavy compact coral limestones, although it might just as well be 
suggested that it is caused by a feeble continuation of the crustal 
