642 KEPOKT— 1881. 



When cemented hy the infiltration of CaOj they are scarcely distinp;uishal)le from 

 some of the older conglomerates. 



Raised beaches exist, between La Scala and Voroldini, between Famagousta and 

 Varoschia, and on the northern coast near the mouth of the river Panagra. The 

 shells found are, for the most part, species now living in the Mediterranean. 



Parts of thf surface of the island are covered with a hard encrustation, known 

 by the name of ' kavara.' The formation of this surface rock is caused by the 

 le-deposition of calcareous matter amongst the gravels, loams, decomposed shales, 

 and other rocks forming the surface soils. 



Blown sands occur on the raised beaches near Famagousta, on the northern 

 coast, and in the valley of the river Angelos, between Myrtu and Morphu, 



The alluvia] deposits consist of sand, gravel, and sandy loams and clays, form- 

 ing rich and fertile land. 



From the character of the rocks now described there is no difficulty in as- 

 signin"' the formation of the Nicosia Beds to Pliocene times. The Miocene age 

 of the Idalian Beds is somewhat more doubtful. Below this all is uncertainty. 

 Hitherto neither the ' Konnos,' nor the Mount Ililarion Limestone, has yielded 

 any fossils. What length of time elapsed between the formation of the compact 

 limestone and the ' Konno=,' or between the ' Konnos ' and the Kerynia Rock, it is 

 impossible to estimate. Failing palfeontological evidence it is impossible to say 

 what formations may be wanting. Lithological characteristics are not implicitly 

 to be depended on, but it is better to give them due consideration thfin to assume 

 a regular succession of formations, as Gaudry has done. Starting from the well- 

 defined horizon of the Nicosia Beds, he classifies the Idalian Beds as Miocene, 

 the 'Konnos' as Eocene, and the Mount Hilarion Limestone as Cretaceous, thus 

 establishing a regular succession in the series. The ' Konnos ' has much litho- 

 loo-ical resemblance to the Vienna Sandstone, and the compact limestone to many 

 of the Jurassic limestones. This classification has been adopted by Unger and 

 Kotschy, and has at least some evidence in its favour. 



The trachyte on which the Idalian Beds rest, on the flanks of the Troodos, 

 appears to be the same rock as occurs at Mavro Vouni, and as appears at different 

 places in the Kerynia range. It is a red, grey, and greenish vesicular and amyg- 

 daloidal trap, traversed by an immense number of joints, filled with calcareous 

 matter, so that the surface of the rock has the appearance of the irregular pave- 

 ment seen in the streets of ancient Roman towns. The lower portion of this 

 trachyte contains beds, veins, or dykes of traps, which stand up above the weathered 

 surface like walls. Below this are found regularly bedded lavas, which surround 

 the serpentines constituting the centre of the Troodos mountain-chain. 



These volcanic rocks, for the most part, have been formed prior to the for- 

 mation of any of the stratified rocks. The invariable occurrence of the amorphous 

 trachyte at so many places on both sides of the central valley, seems to point to 

 its extension under the Tertiary rocks occupying the central portion of the island. 

 There is some metamorphism observable among the stratified rocks near their 

 junction with the trap. This is due to some later action than the formation of the 

 trachyte, as the Idalian Beds rest on its denuded surAice, and outliers of these 

 beds exist at many different places on the flanks of the southern range. The 

 metamorphism is seen in the brown laminated shales with dark chert, in the pink- 

 tinted beds, and in the schistose limestone, and probably dates from the great 

 elevation of the land which took place at the end of Tertiary times. At this 

 period the land was raised, at least, from 1,800 to 2,000 feet. 



Since then an elevation of less extent has occurred. This last upheaval is of 

 comparatively recent date, and not more than 15 or 20 feet in vertical height. 



12. Ohservaiions on the two types of Camlrian hods of the British Isles (the 

 Caledoniali and Hiherno-Camhrimi), and the conditions under which they 

 were respecHvely deposited. By Professor Edwaed Hull, LL.V.,F.B.S. 



In this paper the author pointed out the distinctions in mineral character 

 between the Cambrian beds of the North-West Highlands of Scotland, and their 



