Moldovenesc (Romania) Gheorgheni (Romania) Rakhiv (Ukraine) Vatra Dornei (Romania) Rabka-Zdrój (Poland) Bor (Serbia) Highest peaks This is an (incomplete) list of the peaks of the Carpathians having summits over , with their heights, geologic divisions, and locations. Highest peaks by country This is a list of the highest national peaks of the Carpathians, their heights, geologic divisions, and locations. Excluding mountains located in two countries (on the border). Mountain passes In the Romanian part of the main chain of the Carpathians, mountain passes include Prislop Pass, Tihuța Pass, Bicaz Canyon, Ghimeș Pass, Buzău Pass, Predeal Pass (crossed by the railway from Brașov to Bucharest), Turnu Roșu Pass (1,115 ft., running through the narrow gorge of the Olt River and crossed by the railway from Sibiu to Bucharest), Vulcan Pass, and the Iron Gate (both crossed by the railway from Timișoara to Craiova). Geology The area now occupied by the Carpathians was once occupied by smaller ocean basins. The Carpathian mountains were formed during the Alpine orogeny in the Mesozoic and Tertiary by moving the ALCAPA (Alpine-Carpathian-Pannonian), Tisza and Dacia plates over subducting oceanic crust. The mountains take the form of a fold and thrust belt with generally north vergence in the western segment, northeast to east vergence in the eastern portion and southeast vergence in the southern portion. Currently, the area is the most seismically active in Central Europe. The external, generally northern, portion of the orogenic belt is a Tertiary accretionary wedge of a so-called Flysch belt (the Carpathian Flysch Belt) created by rocks scraped off the sea bottom and thrust over the North-European plate. The Carpathian accretionary wedge is made of several thin skinned nappes composed of Cretaceous to Paleogene turbidites. Thrusting of the Flysch nappes over the Carpathian foreland caused the formation of the Carpathian foreland basin. The boundary between the Flysch belt and internal zones of the orogenic belt in the western segment of the mountain range is marked by the Pieniny Klippen Belt, a narrow complicated zone of polyphase compressional deformation, later involved in a supposed strike-slip zone. Internal zones in western and eastern segments contain older Variscan igneous massifs reworked in Mesozoic thick and thin-skinned nappes. During the Middle Miocene this zone was affected by intensive calc-alkaline arc volcanism that developed over the subduction zone of the flysch basins. At the same time, the internal zones of the orogenic belt were affected by large