25() COL. T. ENGLISH ON THE EOCENE AND [^Ug- I9°4? 



their having been deposited at a point where a further development 

 of synclinal folding subsequently took place. 



Near Myriophy to, on the northern shore^of the Sea of Marmora, 

 a band, full of Ostrea crassissima (Appendix II, p. 285), occurs under 

 soft yellow sand, dipping about 45 c south-south-eastward, at a height 

 of 700 feet above the sea. Below the oyster-band are soft shales, 

 resting upon quartz-conglomerate. The whole of this series has 

 been thrown down by the fault which extends from Mount Elias to 

 Ganos, and abuts on the nearly-vertical Lower Tertiary shales and 

 sandstones (9, p. 152). 



Strata of similar age have been found to the north at Yarna and 

 at Cape Tchokrak in the Kertch Peninsula (18, p. 190, and 24. 

 Table of Beds below the Sarmatic, p. 7), and to the south at Savakly 

 in the Troad (Fischer, 7. pp. 259 et seqq.)\ and at Kasos Island 

 (19, map), and in Thessaly and Macedonia (16, p. 431). 



The Eregli and Myriophyto Lower Miocene marine shell-beds 

 thus form links in a chain of deposits of the same age. extending 

 from the Crimea to the Mediterranean, and the most obvious 

 explanation is that they are detached fragments of what 

 was a continuous sea-bed. 



Between the deposition of these beds and that of the lacustrine 

 and marine Sarmatic strata which succeeded them, the folding 

 must have developed considerably, perhaps to the extent shown 

 in fig. 1, PI. XXII, which indicates the main anticlines of the 

 Eocene and Oligocene Series, and a possible coast-line of the Sarmatic 

 and Pontian basins. 



The connection with the Sarmatic sea probably developed from 

 the outflow of a lake, with a narrow opening to the north-east 

 between the Eocene deposits near Derkos on the Black-Sea coast (see 

 PI. XXI). From here the shore-line swept round the southern 

 portion of the Sea of Marmora, skirting Marmora Island, and the 

 serpentines and schists, volcanic and Eocene strata in the Troad, 

 against which Mr. Calvert has noticed the Sarmatic strata to thin 

 out at Dumbrek in the Kemer Dere, and at Belenkeui. 1 



A deep gulf, directed north-east and south-west, included the 

 Dardanelles and part of Tenedos, and terminated near Mitylene. 

 Its north-western shore skirted the south-east of Imbros and 

 the Oligocene lacustrine sandstones of the Thracian Chersonese, 

 which then formed a long peninsula in the opposite direction to the 

 present one, terminating between Yenikeui and Bulair, where 

 the Sarmatic Beds cross the present isthmus between this point 

 and the Oligocene sandstones near Examil. in what was a channel 

 about 8 miles wide. The waterway was subsequently blocked by 

 the elevation, due to further folding, of the Dohan-Aslan ridge, 

 which is thrown up diagonally across it, and has tilted the 

 bituminous Sarmatic Beds on its southern slope, where they can be 

 seen dipping 50 c south-eastward. 



This channel formed a connection with an internal Sarmatic 



1 Communication to the Author. 



