104 Transactions. 
the oe sheets moved at greater depth, the sea-basins became 
narrower the masses of the geanticlines were pushed forward in a 
nearly Жене direction. . . Such] horizontal movements of the 
curving rows of [East Indian] islands are proved by several features now 
observable on these islands, and as these movements proceed the sea-basins 
be narrowed, and с жены the masses of the present geanticlines 
may уе pushes over the Sahul shelf of the Australian continent." 
This may be illustrated by summarizing the stratigraphical succession 
and the tectonics of certain islands in this Banda arc. rom Timor to 
south-western New Guinea the Permian sediments are of shallow-water 
origin, and are locally interstratified with basic igneous tone Probably 
much of the region was dry land in Permian times. imor the 
Permian sediments pass unbrokenly into Lower лай куче but the 
absence of the latter in other regions bears witness to a general marine 
regression of the sea in Lower Triassic times, followed by a ver 
widespread Upper Triassic transgression. The s ediments were largely of 
on the dde and anticlines of Upper Triassic times, the two facies of 
Triassic rocks being often brought into close apposition by the subsequent 
overthrusting. The Jurassic conditions resembled those of Upper Triassic 
times: the Jurassic sediments are partly those of deep-sea origin, bu 
shallow-water deposits only occur in Misol and the Sula Islands. These 
general conditions continued up into Lower Cretaceous times, with 
apparently numerous local lacunae in the sequence of strata, the diversity 
of sedimentary facies resulting from the constant formation of geanticlinal 
ridges on which neritic sediments were deposited, and which were thrust 
forward along gently inclined planes of faulting at geosynclinal depths. 
These crust-movements were very marked in Cretaceous times, when the 
sea retreated from much of the present East Indian land-areas. The free 
connection between the eastern Australasian region and the Tethys was 
broken (Martin, 1914), and numerous plutonic intrusions were formed. 
It is difficult to state exactly the directions of strike of these late Mesozoic 
folds, for they have been greatly modified by the later Miocene orogeny. 
e orogenic stresses being temporarily relieved, a general subsidence 
occurred with the transgression of a shallow sea over Rotti, Timor, 
Letti, Ceram, and Buru, depositing Upper Cretaceous foraminiferal marls, 
accompanied by the formation of more littoral deposits in Celebes. This 
transgression was further extended in early Tertiary times, and the 
deposits formed were more diversified—littoral conglomerates, sandstones, 
Sumbawa, Flores, and Sumba is a large amount of andesitic débris. The 
formation of ман e deep-sea basins and other crust-movements began 
‘п Miocene ti 
Tertiary geanticlines. The phenomena of klippen (or, as the Dutch 
geologists prefer to call them, fatus, using the local Malayan term) аге 
clearly developed: “ Groups of deposits of the same age but of different 
жеанын) and petrographical character are found one on top of the 
