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Geology af Albanides
THE ADVENTURES OF A NOTION: ALBANIDES
On the 1883 E. Sues denominated as Dinarides "the mountain System which extends in the western part of Balkan Peninsula"
On the 1901 J. Cvijic denominated as "Dinarische-Albanesische Scharung" the bending of the Dinaric structures m the Shkodra region, just there which nowadays is world-wide known as the Shkodėr-Pejė transverse structure. On the 1922 G. Dainelli subdivided explicitly, but roughly the Dinarides in a northern part, which he named as Dinaric Alps ( Dinarides s.s) and in the another southern part, which he called as Albanian Alps. He meant through this term not only the Alps of Northern Albania, but the whole geological structures of Albania, which are connected, farther to the south, with the Pindos.
On the 1929 L. Kober (4) 4 zones are distingue in the whole Dinarides (s.l.) between Trieste and the Aegean Sea. As far as it concerns the western zone, which includes also the Marginal Adriatic Ranges, Kober underlines the fact that near the " Albanesische Scharung" the structural trend changes and has a more meridional, north-south direction.
According to Kober, in this areas "Beside of Marginal Adriatic Zone is clearly delineated the Hellenic Zone, if it could be called so" (Op. cit., p. 427). And he concluded underlying that the "This extremely Dinaric-Hellenic zone, perhaps may be named commonly as Ionides..... The Shkodėr bend divides the Ionides into to sectors: in one Adriatic sector and another Hellenic sector. We must pay much attention to this strange structure. "French has been right to divide the Dinarides and the Hellenides" (Op. cit., p. 429)
No what does French say? In his Work ( 4 ) he made a synthesis for the geological framework of Balkan Peninsula and underlined just on 1909 (Op. cit, p.653) that "The Dinarides of Shkodėr continue with the Albano-Hellenic Mountains ("Albano- Hellenische Gebirge") and that (Op. cit., p.656) "The limit of the Dinarides with this Mountains is clear enough". It is evident that French on 1909 has not formally divided the Dinarides and the Hellenides, as Kober pretended. Consequently this division is made by L. Kober himself on 1929, without taking in consideration the previous denominations by French ("Albano-Hellenic Mountains") and G. Dainelli ("Albanian Alps"), which have a scientific priority. However the Kobers subdivision of the Dinarides (s.l.) remained in the geological literature and was widely used, especially in the works of 50th and 60th years.
On the 1967, Luan Peza suggested the term Albanide to be used "for the assemblage of Albanian geological structures". This term began at once to be used from the albanian geologist. In the Workshop of the Dinarides, held at Paris, December, 1970, A. Papa augmented the necessity of using the term "Albanides", because the subdivision of the Dinarides (s.Z.) in two segments occurs within the Albanian territory. Worldwide known geologists, as J. Aubouin, have not opposed this argument, but underlined the difficulty to change a terminology being already used for long time in the European geological literature.
Afterwards, in the 80th particularly in the 90th, as is clearly evident, especially in the works of the Workshop of the Geology of Albania, held in Paris on April 1991, the term AIbanides began gradually to get the right of citizenship. This term was used in the papers of albanian geologists, in the joint papers of albanian and other european geologists and, finally, in many papers written by european geologists.
In the 90th in many publications of albanian geologists, such as K. Gjata, A. Kodra, Dh. Tagari, and m their papers with other european co-authors, began to be used the term "Dinaric- Albanian-Hellenic-Arc" (Ensemble) for the denomination of the Dinarides. Our view is that the first division responded better to the contemporaneous concepts of plate tectonics and respects the scientific priority, for the subdivision of the Dinarides (s.l.) in the closely linked segments. With the "at outs" which it has, even the term Dinaric-Albanian- Hellenic Arc will gradually began to get more ground.
Asti PAPA, Association of Albanian Geologist
Albanides
The Albanides are continuity of Dinaride northwards and Hellenide southwards. High tectonic
The division in tectonic zones is based on the stratigraphic, structural data and relevant criteria used about this division.
Used criteria are the facial, structural, age of the tectogenese, intensity of magmatism, relationships between tectonic units etc.
Based on such criteria, Albandes are divided into inner and outer tectonic zones as follow:
Inner zones
1. Korabi zone (Ko)
2. Gashi Zone (G)
3. Mirdita zone (M)
3.a) Ophiolitic sub zone (M1)
3.b) Carbonate sub zone (M2)
Outers zones
1. Albanian Alps zone (A),
1a) Malesia e Madhe sub zone (A1)
2b) Valbona Sub zone (A2)
2. Krasta Cukali zone (K-C)
2a) Cukali sub zonet (K-C1)
2b) Krasta sub zone (K-C2)
2c) Dibra unit (K-C3)
2d) Spiten-Lisna unit (K-C4)
2e) Vermoshi unit (K-C5)
3. Kruja zone (K)
4. Ionian zone (J)
5. Sazani zone (S)
6. The unit of molasses deposits of inners depressions (Gr)
7. The unit of molasses deposits of Preadriatic depression (U)
8. Evaporates unit
Concepts over the Cermenika zone
Some authors have proposed to include the Cermenica zone as a new zone of Albanides based on:
Presence, of condensed carbonate-siliceous and siliceous-pelagic deposits, of Jurassic age, in the ophiolitic cross section.
Presence and regional spreading of the conglo-breccious and flyschoidal deposits, belong to the Jurassic-Cretaceous border.
Paleogeographic and geotectonic evolution of Eastern Albanides, where the ophiolites are formed by the plates movement mechanism.
Characteristics of geologic configuration of Albanides
The structural direction is northwestern, but the Shkoder-Peje transform fault, has a deviation from this direction
Albanides represent a important structural and formational sector, in the frame of the ophiolitic magmatism evolution.
Albanides are characterized by folded structures.
Is observed the development of both, overthrust and covering tectonic.
Characteristic is the migration of flysch from the east to west.
Involved by two orogenic cycles: varisic and alpin and from several fazes of tectogenesis.
Relatively high seismic activity.
Several transform faults as: Shoder-Peje (Scutari-Pec), Labinot-Dibėr, Fierzė-Poravė-Kukės, Lushnjė-Elbasan-Librazhd etc.
Albanides as part of the Alpine Orogenic System
Albania is part of the sectors of the Alpin and Neo-European system. Albanides are part of the Dinaric-Albanidic-Helenic arc, this chain is part of the orogenic Alpine chain that continue till, at the Himalaya ensemble. The highest worlds picks founded here. This zone incurs a powerful up rise, caused by the collision of EuroAsia plate in north with the African, Arabic and Indian plates in south (Gondwanaland).
The orogenic chain Alps-Himalaya is formed by folding and deposits during the Mesozoic period, and partially during Cenozoic period in a large oceand between the two continents EuroAsia and Gondwanaland, well known as Tethys. So, the Tethyan system is composed by mountain chains, from the Alps to Himalaya. Alias is called as Tethyan Orogenic System.
In this system is included and the Dinaric-Albanic-Hellenic arc, bordered eastward by faults with the central massifs of Panonia, Serb-Macedonian, Rodope, Ciclades and westward with the plunged central massif Ardiratic-Ionian. This arc supposed to begin from the Julian Alps (Italy-Slovenia), with a tectonic contact, where the massifs are plunged down, creating deep faults for magmatic infiltrations. The arc direction is northwestern and is complicated by the Shkoder-Peje transform fault.
This arc is characterized by many types of formations, facie, structures where distinguished tectonic series, that divide this arc into inner and outer zones, based on the magmatic processes. The inner zones of the arc show a great magmatic activity, meantime in the outer this activity is insignificant or absent.
The tectonic zones of the Dinaric-Albanic-Hellenic arc.
Pelagonian zone is situated in Helenides, with analogs Korabi zone in Albanides and Durmitori zone in Dinarides. This zone have a tectonically bordered with Vardari and Subpelagonian zones. In Macedonia represent metamorphic formations of the Precambrian age divided into two complexes: the lower composed by gneisses and micaceous shale, and the upper composed by a mixed series and marls. Paleozoic formations are represented by clay shale, phyllite, sandstone and limestone metamorphosed lens with brachiopods and crinoids. Encountered ophiolites of the upper Jurassic, and Cretaceous depositions with rudists covered by flysch.
Serbian zone such knowed in Dinarides, meantime in Albanides is known as Mirdita zone and Subpelagonian zone in Helenides. Is a ophiolitic zone, characterized from outcrops of shale, sandstone and lower Carboniferous limestone lenses covered inconsistency by a thin sandstone packet of Verrucano type. Up appear Triassic-Jurassic limestone followed by Cretaceous depositions from that the upper Cretaceous is most developed than the lower one. The Tertiary is represented by andesitic volcanism. In the Serbian zone (Dinarides) they have a aloctone nature of the tectonic style. Ultrabasic rocks over thrust as tablets over the diabase-radiolarites or limestone. In Helenides encountered the ammonitico rosso of Ladinian that is followed by limestone of the upper Triassic-lower Jurassic and siliceous packet of upper Jurassic. There founded transgresive limestone of Cretaceous. The Oligocene and Miocene are composed by molasses.
Bosnian Unit. Recently in Dinarides called as "Bosnian Zone" or "Bosnian Flysch". The depositions of this zone are neritic limestones, follwed by radiolaritic packet, upper limestone with cadosina that is followed by the authentic Biosnian flysch. This is followed by a second flysh with limestone conjunction.
Beotian zone is situated between Inner and Outer Helenides and is comprehend between Subpelagonian and Parnas-Giona zones. The depositions are represented by limestone and dolomite belong to Triassic-middle Jurassic, up is situated the amonitico rosso, upper this situated a radiolaritic packet of the middle-upper Jurassic, covered by the flysch, and after follows the Cretaceous limestone and Tertiary flysch.
Parnas-Gijona zone is known with this name i Helenides, in Dinarides is known as High Karts zone and in Albanides as Albanian Alps zone. Is covered tectonically eastward by Subpelagonian zone, and westwards over thrust the Pindos zone. The depositions represented by dolomites and limestone of lower Triassic, dark color limestone of lower Triassic, oolitic limestone of the middle Jurassic, followed by different packets of limestone and upper found the flysch of the Paleocene-Eocene.
Pindos zone is known with this name in Helenides, known as Budva zone in Dinarides and as Krasta-Cukali zone in Albanides. This zone is situated tectonicali over the Gavrovo zone. Is composed by limestone with siliceous, shale and siliceous that continue with the early flysch of the Barremian-lower Turonian followed by limestone of the upper turonian-cenomanian followed by the second flysch of the Paleocene-Eocene. Meantime in Budva zone found depositions of Verfenian where limestone blocks are situated which supposed to belong to Permian. Upper there is situated the Anisian flysch upper this is the porfirit-radiolaritic Ladinian and after pelagic limestone further cretaceous siliceous limestone followed by flysh of Danian-Eocene.
Gavrovo zone is known with this name in Helenides, meantime in Dinarides is known as Dalmatian zone and in Abanides as Kruja zone. Situated over Pindos and Ionian zones, and have tectonic overthrust relationships with them. The depositions are represented by different limestone packets of Triassic-Cretaceous-Eocene and upper those follow the flysch of Oligocene-Aquitaniane. Meantime in Dalmatian zone the flysh begin in the upper Eocene.
Paxos zone is known with this this name in Helenides, and as sazani zone in Albanides. Doesnt exist at Dinarides. In Italy but and in Helenides is know and as Pre-Apulian zone. This zone have represent a ridge situated over the hercynian basement of the upraised central massif of Adriatic, that was bordered eastwards by the Ionian through, and westwards by the Umbre-Marke through. Is characterized by continues carbonate deposition, mainly neritic during whole the Cretaceous and Paleogene, and from flysch absence. The Preapulian zone was represented by calcareous marl, or authentic marl. Tectonically represent a thick packet situated mainly horizontally with almost horizontal tectonic thrusts.
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External Zones |
HELENIDET |
ALBANIDET |
DINARIDET |
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Pre-Apulian zone |
Sazani zone |
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Jonian zone |
Jonian zone |
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Gavrovo zone |
Kruja zone |
Dalmatian zone |
|
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Pindus zone |
Krasta-Cukali zone |
Budva zone |
|
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Parnassus zone |
Albanian Alps zone (Malėsie e Madhe s/zone Valbona s/zone) |
High-Krast zone Pre-Karst zone |
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Internal Zones |
Sub-Pelagonian zone (Maliac) |
Mirdita zone |
Serbian zone |
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Pelagonian zone |
Korabi zone |
Golija zone |
|
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Vardari zone |
Vardari zone |
Paleogeography of Albanides
The Development of Albanides is known from Ordivocian-Devonian period. The Mirdita and Korabi zones during this period were part of a continental crust.
The configuration via vertical movements was very complicated with through and ridge.
The Kollovozi unit during Ordovician was a neritic basin with sedimentation of conglomerates, arenaceous, alevrolites and mud sedimentations.
During Silurian is happened a deepening of basin. In the Kollovozi unit we have mudstone strata reached with organic material as graptolites and limestone strata with conodontes. In the Muhurri unit in neritic conditions are formed mudstones with graptolites.
In Devonian is happened the deepening of basin as during Silurian, but here the limestone depositions reached with crinoids, bivalve, tentaculides and orthoceratites is grow.
The existence of Carboniferous is not evidenced by the researches.
During Permian-Verfenian (Lower Triassic) sectors of Albanides was covered by an epicontinental sea. In the outer zones was begin the rifting process, which has as conclusion the salt deposits that belong today to Peshkopia, Dumrea etc. In the Alps zone are sediment the carbonatic-terrigenous formations reached with fusulinides and foraminifera. During this period cause of magmatism appear the plutonic rocks presented by dike series and gabbro-diabases.
During Anisian (Lower Triassic) the same paleogeographical process as in Verfenian was continued. Here are sedimented carbonates reached in pelagic bivalves, ammonites and foraminifera, testimony for a deepening of the basin and a powerful volcanic activity.
During Ladinian was happened the differentiation of the basin in the platformic and basin (pelagic) sectors. The zone of Korabi was in pelagic conditions were limestone with bivalve was deposited. The Mirdita zone in plat formic conditions was composed by algaceous limestone. Albanian Alps zone was a platform that during the end of Ladinian was partially outcropped. In the Sazani zone in neritic conditions we have neritic depositions, meantime the Ionian zone was represented by a through where the basin differentiation was emerged.
During Upper Triassic in The Albanian Alps zone was appeared a shallow sea where was accumulated carbonate sediments reached in algae and megalodontes.
During Upper Triassic-Lower Jurassic the Mirdita zone was in neritic conditions with sedimentation of limestone with megalodontes and stromatilythic limestone. In Korabi zone in neritic conditions the deposits of the limestone with bivalve was continued. The Alps zone is remained still in neritic conditions. The Cukali sub zone is found in basin conditions with carbonate-siliceous depositions, meantime the Lisne-Spien unit (belong to Krasta sub zone) was represented as offset sector composed by limestone reached in megalodontes.
During the Lower Jurassic the Albanian Alps continue to be found in the shallow waters conditions where the neritic sediment was composed by limestone with protodiceras and litiotides. The Sazani zone and may be a Kruja are in neritic conditions. At the last of the lower Jurassic in the Mirdita and Korabi zones, in some sector the pelagic condition was appeared with carbonate-siliceous formations. In the Alps, notified a general deepening, with the appearance of the siliceous limestone. The Ionian through take the full aspect separating by the ridges of Sazani and Kruja.
During the Middle Jurassic the Ionian zone is continued the deepening with the sedimentation of algaceous limestone.
During the Middle-Upper Jurassic by the effect of the ocean enlargement was formed the ophiolites with volcanogenic and plutogene facie. During this period in Cukali subzone have a deposition of limestone and radiolaritic siliceous. In the Alps zone we have a full differentiation of the both sub zones; Malesia e Madhe and Valbona. In the Malesia e Madhe have neritic limestone sedimentation, meantime in the Valbona limestone of the slope facie. Is supposed that, during Jurassic, the Kruja zone have represented a platform with neritic sedimentation. The Ionian zone continues to deepening and sediments of limestone with saccocoma.
During Cretaceous (Berriasian-Valanzhinian), a pelagic sea cover a large area, where except the breccia sediments are noted turbitic sediments. During Barremnian have a general shallow of the Mirdita and Korabi zones and have a pass by pelagic sediments in shallow one. During this era are distinguished conglomeratic, sandy and marly sedimentations that comprehend bivalve and gastropods. During albian-senomanian is passed in neritic carbonate depositions. Malesia e Madhe sub zone represent a ridge in continue plunging reached with neritc limestone with rudiste. Valbona sub zone represent a slope with sedimentation of turbiditic limestones with calpionelides. Krasta-Cukali represent a pelagic sea with limestone mud, meantime Kruja zone was a ridge in process of plunging with carbonatic material. Ionian zone represent a through with pelagic carbonate sediments, meantime Sazani zone was a plat form in plunging with algaceous limestones.
During Paleocene-Eocene the Mirdita and Korabi zones was emerge up the water surface. In the Mirdita zone have the terrigenous flysch sedimentation with globorotaria and globigerina. And the Alps were emerged on surface during this period. Krasta-Cukali represent a basin with pelagic sediments such mudstone-alevrolitic and carbonate-marl with globorotaria and globigerina. Kruja zone represented by a ridge with a accidence relief, that at the last of Paleocene was almost emerged. In the Ionian zone have sedimentation of turbid tic limestone, meantime Sazani zone was emerged until middle Eocene and after was plunged and biomicritic limestone was sedimented reached in nummulites, discoclyna etc.
During Oligocene the Krasta sub zone was emerged. The Kruja zone represented the same basin with the Ionian zone, where was amalgamate terrigenous sediments. In the Ionian zone have a general deepening in which was appear the aracenous-mud sediments of the eastern sectors of the basin. During middle Oligocene the eastern parts of the Kruaj zone supposed to be emerged, are plunged again during the upper Oligocene. Sazani zone was a ridge with carbonate sedimentation reached with benthonic foraminifera.
In Neogenes, during Aquitaine in Ionian zone the basin swallowed continually. The Sazani zone plugged again and begins to sediment mud-siltstone-sandy material wit plankton foraminifera. During Burdigalian Mirdita zone reduce the terrigenous material and pass in carbonatic one, meantime the Ionian zone continue the general deepening of the basin composed by pelagic sediments, and those sediments with foraminifera continue and during Helvetian. Sazani zone was covered by the sea and in such pelagic conditions over the Cretaceous limestone was established marls and clays. During Helvetian the Mirdita Kruja and Krasta-Cukali zones emerged. During Tortonian have a shallow of the basin of the Ionian zone with marl sediment. The outer zones and the Ionian zone were involved by foded processes. After the plunging of the Adriatic plate under the orogene between Shkoder-Peje and Vlore-Tepelene faults the Pre Adriatic Depression was formed (Tortonian).
In the western part of the Depression the basin was very deep. The sea infiltred from the north-northwest and east-southeast located up the northwestern area of the Ionian zone, where the have clay sediments 3000m thickening. Also the transgression of Tortonian was infiltrated in the Inner Depression of Librazhdi and Burreli. In the Burreli Depression was a lake basin with conglomeratic, sandy, clay and coal sediments.
During Mesinian in the Preadriatic Depression the sea was departed. From east to west an increase of the salinity is remarked. This and the closed sea create the conditions of evaporates forming.
In the lower Pliocene (upper Neogene) we notice a folding faze that form the structures of the Preadriatic Depression and include the inner Depressions to. The Mirdita zone incurs an enlargement, and as result tectonic depressions was created (in Korca, Peshkopia, Tropoja). The sediments are clay-sandy and conglomerates with coal strata.
During middle Pliocene the Depression incure a plunging and the sea extended eastern. The sediments are conglomerate-sandy coastal and pelagic. The transgression of Pliocene is remarked and in the Krasta-Cukali and Albanian Alps zone. The sea is ifiltred mainlz in the paleovalley of Drini River and Kopliku lowland. In the Preadriatic Depresion at the end of Pliocene found regressive series characterized with diminution of platonic foraminifera. The genius Amonia is dominated.
The actually configuration of Albanides from the orogenic movements belong to Pliocene-Quaternary. The sedimentation is terrigenous in the lake-fen conditions and continue in the Pliocene-Quaternary depressions of the Mirdita zone.
CORRELATION OF THE GEOLOGICAL MAPS 1:50 000 SCALE OF THE ALBANIAN - NEIGHBOURING COUNTRIES BORDER AREA
Some joint projects to unify the main data on the geological-tectonic structures, lithological composition and the ages of the formations on both sides of the border between the countries, have been undertaken these last years and the results are encouraging. The mutual cooperation between the respective scientific institutions is very important taking into account the participation of both countries in the compilation of the New Geological Map of Europe 1:500 000 scale.
The implementation of the 1:50 000 scale mappings of the border area is indispensable. The correlation of these maps is realized through geological observations, sampling and other geological works. The implementation of the new geological maps 1:50 000 will serve as a good scientific basis for further studies in the field of earth sciences in the region.
The common observations and geological investigations along the interboundary line have leaded to the correlation of the Ionian, Kruja (Gavrovo), Krasta-Cukali (Ollonos-Pindos), Mirdita (Subpelagonian) tectonic zones and Inner Depressions as well as the correlation of the geological and ore bearing structures and other formations along the respective inter-boundary line.
The comparison of data on the stratigraphy, petrology, mineralogy etc., of different geological units has been carried out as well.
During this cooperation it is worked with topographic sheets scale 1:50 000, on which were plotted the geological data in digital form (using AutoCAD Map 2000 and MicroStation software).
The final result is the publication of 38 geological sheets 1:50 000 scale and explanatory texts for each of them, for all the inter-boundary line between the countries. The following unified sheets 1:50 000 scales were published:
Albanian-Montenegro border area
1. Sheet 1 Vermoshi
2. Sheet 2 Gucia
3. Sheet 3 Stanet e Sublices.
4. Sheet 4 Rapsh-Starja
5 Sheet 5 Tamara
6. Sheet 6 Thethi
7. Sheet 8 Kopliku
8. Sheet 14 Shiroka
9. Sheet 20 Velipoja
Albanian- Kosovo border area
1. Sheet 7 Bajram Curri
2. Sheet 12 Kruma
3. Sheet 13 Kishaj
4. Sheet 19 Morini
Albanian- Macedonia border area
1 Sheet 25 Shishtaveci
2. Sheet 30 Mali i Korabit
3. Sheet 35 Zerqani
4. Sheet 36 Poēesti
5. Sheet 41 Klenja
6. Sheet 42 Trebishti
7. Sheet 47 Librazhdi
8. Sheet 48 Struga
9 Sheet 54 Prrenjasi
10. Sheet 60 Pogradeci.
11. Sheet 61 Bllaca.
Albanian-Greece border area
1. Sheet 68 Pojani-Podgori Andartikon
2. Shee 69 Shueci Andartikon
3. Sheet 76 Korca-Hionades Gramos
4. Sheet 77 Kapshtica- Korica Massapotamia
5. Sheet 84 Vidohova Hionades Gramos
6. Sheet 90 Barmash-Hionades Gramos-Vassilikon Pogoniani
7. Sheet 91 Hionades Gramos-Vassilikon Pogoniani
8. Sheet 95 Libohova- Tsamantas
9. Sheet 96 Leskoviku-Hioandes Gramos- Vassilikon Pogoniani
10. Sheet 99 Jergucati-Tsamantas
11 Sheet 100 Ksamili-Ishulli i Korfuzit
12. Sheet 101 Mursia-Tsamantas
13. Sheet 102 Sotira-Tsamantas
14. Sheet 103 Konispoli-Sagiadha-Filatai
There have been compiled and published the inter-boundary geological maps scale 1:50 000.
Scientific interpretation of geological phenomena based on modern approaches.
Compilation of a database aiming to the planning of a rational national management and exploitation of raw materials, water resources, environmental protection, ore minerals etc.
The geological maps 1:50 000 scales will be useful to various geo-scientific institutions (public and private) in both countries, in the Balkan region and in Europe.
Some data about Geological Map on scale 1:50 000
By Prof.as.Dr. Kujtim Onuzi
Geological maps on scale 1:50 000 until 2006