16 Water Resources from Apuseni Mountains …
535
processes, like humidity discharges and weather disturbances, which will generate a
genuine valley topoclimate [63].
B˘ atrâna Mountains, a toponym from the dominant peak (1579 m), represents the
orographic point in the central part of the Apuseni Mountains, but also a hydrographical boundary because it separates the basin of Cri¸ sul Pietros, Some¸ sul Cald
and Arie¸ s river. The fundamental characteristics are imposed by the geological constitution marked by the intercalation of crystalline rocks, with sedimentary rocks,
especially limestone and dolomite (Fig. 16.5). The alternation in stripes of noncarstificable rocks (75.3%) with carstifiable rocks led to the emergence of seamless
peaks, depressions and relatively low plateaus, the latter dominated by endo and
exocartst shapes (caves, avenues, valleys, etc.) [13].
Viewed as a whole, the mountain ridges are arranged on different levels: at
1500–1600 m there are residual peaks from an old peneplena (M˘ agura Vân˘ at˘ a 1641 m,
B˘ atrâna peak 1579 m), followed by a lower level 1400–1500 m (Piatra Burned
1488 m, Mo¸ tului Church 1466 m), but related to the same period of carving, the
M˘ aguri-M˘ ari¸ sel polyclinic complex. The carstifiable formations have enriched the
old surface by generating depressions and plateaux considered as carstoplen remains
(Padis , plateau). At 1000–1100 m there are extensive heights, shaped on crystalline
schist and granite. This step represents the mountain that has entered strong under
the human impact: settlements, pastures, roads, etc. [46].
Muntele Mare Mountains are based on an old hercynian age chain, cut and then
peneplenized, covered with large waters in the paleogene and raised again into
neogen. Built like a monolithic giant block through the center of its granite platoon, it features a dominant relief of rounded ridges with smooth or slightly curled
surfaces, contrasted with the depths of the valleys and the high slopes of the valleys’
sides. It is the area known in the literature as the M˘ ari¸ sel Platform (1200–1600 m),
which after deforestations were established crops, the crâng households, resulting
in an active human life [46].
Gil˘ au Mountains are considered an extension to the north of Muntele Mare massif, at a lower altitude (1600–1200 m). The area of their maximum deployment is
represented by the interfluvium separating the water catchment area of Some¸ sul Cald
from Cri¸ sul Repede one [63].
Also constituted from resistant rocks (crystalline shale), the relief of the Gil˘ au
Mountains has the same physiognomy of slightly wavy and smooth ridges. The
north-eastern tilting direction of the whole mass is underlined by the decrease of the
altitudes from 1692 m (Cârliga¸ ti peak—hydrographic crossing point in the Apuseni
Mountains), 1649 m (Cump˘ an˘ a¸ telu peak), 1404 m (C˘ al˘ a¸ tele Hill), 1099 m (Dealu
Negru), near the village of Belis , and only 900 m on the ridges that surround the town
of R⸠sca.
As a result of external agents action started in Danian age, three levels of relief
modeling were finalized. The upper level (called F˘ arca¸ s-Cârliga¸ ti) is situated at
1400–1800 m, was modeled in Danian-Oligocen period. The middle level (MaguriM˘ ari¸ sel), more fragmented than the first one, is situated at 1200–1400 m and was
modeled in Sarmatian-Meotian period. The lowest level of Pliocen-Quaternary age
(called Fene¸ s-Deva), appears in the form of shoulders along the valleys entering the
535
processes, like humidity discharges and weather disturbances, which will generate a
genuine valley topoclimate [63].
B˘ atrâna Mountains, a toponym from the dominant peak (1579 m), represents the
orographic point in the central part of the Apuseni Mountains, but also a hydrographical boundary because it separates the basin of Cri¸ sul Pietros, Some¸ sul Cald
and Arie¸ s river. The fundamental characteristics are imposed by the geological constitution marked by the intercalation of crystalline rocks, with sedimentary rocks,
especially limestone and dolomite (Fig. 16.5). The alternation in stripes of noncarstificable rocks (75.3%) with carstifiable rocks led to the emergence of seamless
peaks, depressions and relatively low plateaus, the latter dominated by endo and
exocartst shapes (caves, avenues, valleys, etc.) [13].
Viewed as a whole, the mountain ridges are arranged on different levels: at
1500–1600 m there are residual peaks from an old peneplena (M˘ agura Vân˘ at˘ a 1641 m,
B˘ atrâna peak 1579 m), followed by a lower level 1400–1500 m (Piatra Burned
1488 m, Mo¸ tului Church 1466 m), but related to the same period of carving, the
M˘ aguri-M˘ ari¸ sel polyclinic complex. The carstifiable formations have enriched the
old surface by generating depressions and plateaux considered as carstoplen remains
(Padis , plateau). At 1000–1100 m there are extensive heights, shaped on crystalline
schist and granite. This step represents the mountain that has entered strong under
the human impact: settlements, pastures, roads, etc. [46].
Muntele Mare Mountains are based on an old hercynian age chain, cut and then
peneplenized, covered with large waters in the paleogene and raised again into
neogen. Built like a monolithic giant block through the center of its granite platoon, it features a dominant relief of rounded ridges with smooth or slightly curled
surfaces, contrasted with the depths of the valleys and the high slopes of the valleys’
sides. It is the area known in the literature as the M˘ ari¸ sel Platform (1200–1600 m),
which after deforestations were established crops, the crâng households, resulting
in an active human life [46].
Gil˘ au Mountains are considered an extension to the north of Muntele Mare massif, at a lower altitude (1600–1200 m). The area of their maximum deployment is
represented by the interfluvium separating the water catchment area of Some¸ sul Cald
from Cri¸ sul Repede one [63].
Also constituted from resistant rocks (crystalline shale), the relief of the Gil˘ au
Mountains has the same physiognomy of slightly wavy and smooth ridges. The
north-eastern tilting direction of the whole mass is underlined by the decrease of the
altitudes from 1692 m (Cârliga¸ ti peak—hydrographic crossing point in the Apuseni
Mountains), 1649 m (Cump˘ an˘ a¸ telu peak), 1404 m (C˘ al˘ a¸ tele Hill), 1099 m (Dealu
Negru), near the village of Belis , and only 900 m on the ridges that surround the town
of R⸠sca.
As a result of external agents action started in Danian age, three levels of relief
modeling were finalized. The upper level (called F˘ arca¸ s-Cârliga¸ ti) is situated at
1400–1800 m, was modeled in Danian-Oligocen period. The middle level (MaguriM˘ ari¸ sel), more fragmented than the first one, is situated at 1200–1400 m and was
modeled in Sarmatian-Meotian period. The lowest level of Pliocen-Quaternary age
(called Fene¸ s-Deva), appears in the form of shoulders along the valleys entering the