The Alpine Late Collisional Rila-Rhodope Metallogenic Zone of the Balkan Orogenic System

СПИСАНИЕ НА БЪЛГАРСКОТО ГЕОЛОГИЧЕСКО ДРУЖЕСТВО, год. 80, кн. 1, 2019, с. 55–79 REVIEW OF THE BULGARIAN GEOLOGICAL SOCIETY, vol. 80, part 1, 2019, p. 55–79

The Alpine late collisional Rila-Rhodope Metallogenic Zone of the Balkan Orogenic System

Kamen Popov, Petko Popov

University of Mining and Geology “St. Ivan Rilski”, Department of Geology and Exploration of Mineral Deposits, 1 Prof. Boyan Kamenov str., Studentski Grad, 1700 Sofia, Bulgaria; E-mail: [email protected]

Алпийската късноколизионна Рило-Родопска металогенна зона в Балканската орогенна система

Камен Попов, Петко Попов

Минно-геоложки университет „Св. Иван Рилски“, Катедра „Геология и проучване на полезни изкопаеми“, Студентски град, ул. „Проф. Боян Каменов“ № 1, София 1700

Резюме. В еволюцията на Балканската орогенна система, като част от Алпо-Хималайския пояс, се проявява стадий на коли- зионни процеси, обхващащи врeмето от Mастрихта до Лютеса. В северните части на системата е разположено субекваториалното Кула-Обзорско предпланинско понижение с палеоцен-лютеска плиткоморска ритмична моласа, а на юг – бартон-плиоценски континентални наслаги. В южните части на орогенната система се внедряват плутони, обособени като горномастрихт-лютески Рилo-Родопски комплекс, вместени в метаморфитите от фундамента. Колизионният стадий завършва с илирските гънкови и възседно-навлачни деформации. Металогенните процеси са свързани с горномастрихт-лютеския магмен комплекс. Образувана е поредица от рудни находища, определящи позицията на Рило-Родопската металогенна зона. Те се характеризират с преоблада- ващото развитие на хидротермални руди на волфрам, молибден, уран и на флуорит. Освен това присъстват железни, злато-анти- монови, бисмутови и по-рядко полиметални, злато-полиметални и медни минерализации. Често те са с близки пространствени, темпорални и минeрало-геохимични връзки. Очертават се Рило-Западнородопският, Ракитовско-Бачковският и Барутинско- Смилянският руден район, в които се обособяват отделни рудни полета или рудни минерализирани площи.

Ключови думи: Балканска алпийска система, илирска колизия (Лютес), горномастрихт-лютески гранитоиден комплекс, Рило-Родопска металогенна зона, W, Mo, флуоритови, U и Sb (+Au) находища.

Abstract. During the Late Maastrichtian to the Lutetian time, a stage of collisional processes has occurred in the evolution of the Balkan Orogenic System, which is a part of the Alpine-Himalayan belt. The subequatorial Kula-Obzor Foredeep with Paleocene–Lutetian shallow marine rhythmic molasse is situated in the northern parts of the system, while the Barthonian–Pliocene continental sediments are deposited to the south. Paleocene–Lutetian plutons are developed in the southern parts of the orogenic system and they are nominated as Rila-Rhodope Upper Maastrichtian–Lutetian complex, intruded within the metamorphic rocks of the basement. The collisional stage terminates with the Illyrian fold and thrust-nappe deformations. The metallogenic processes are related to the Upper Maastrichtian–Lutetian magmatic complex. Numerous ore deposits are formed, thus defining the position of the Rila-Rhodope metallogenic zone. They are characterized by the predominant development of hydrothermal W, Mo, U ores and fluorite. Fe, Sb (+Au), Bi, and rarely polymetallic, Au-polymetallic and Cu mineralizations are represented as well. Often they are in close spatial, temporal and mineralogical-geochemical relations. Rila-Western Rhodope, Rakitovo-Bachkovo and Barutin-Smilyan ore regions are defined and individual ore fields or mineralized ore areas are differentiated within them.

Keywords: Balkan Alpine System, Illyrian сollision (Lutetian), Upper Maastrichtian–Lutetian granitoid complex, Rila- Rhodope metallogenic zone, W, Mo, fluorite, U, Sb (+Au) deposits.

Introduction continental blocks. The Balkan, Srednogorie and Morava-Rhodope Zones are situated between the The Balkan Orogenic System (the Balkanides) is a Moesian Platform and the Vardar suture (Dabovski, part of the Alpine-Himalayan belt and it is formed Zagorcev, 2009). Practically, all researchers agreed in the active SE margin of the Paleo-European that the Balkan tectonic system is developed along continent, subparallel to the Vardar Paleo-ocean the NE continental board of the Vardar Paleo-ocean, (Fig. 1). The evolution of the tectonic system is and the southern flank of the Moesian Platform. marked by sequence of tectonic events leading to Different authors distinguish subsequent stages of the paleo-ocean’s closure and collision between the ocean rifting, subduction and Austrian collision,

55 Fig. 1. Geologic scheme of Bulgaria for the Alpine collisional stage (Maastrichtian–Lutetian) 1, epicontinental Bartonian–Quaternary sediments; 2, Paleocene–Lutetian granitoid rocks; 3, Paleocene–Lutetian foothill sediments; 4, Mesozoic basement; 5, Paleozoic–Neoproterozoic basement; 6, Krumovgrad terrigenous continental basin; 7, Kula- Obzor Foredeep Фиг. 1. Геоложка схема на България за алпийския колизионен етап (Мастрихт–Лютес) 1 – епиконтинентални бартон-кватернерни отложения; 2 – палеоцен-лютески гранитоидни скали; 3 – предпланински па- леоцен-лютески седименти; 4 – мезозойска подложка; 5 – палеозой-неопротерозойски фундамент; 6 – Крумовградски теригенен континентален басейн; 7 – Кула-Обзорско предпланинско понижение

Late Cretaceous mantle-crustal magmatism with purposes. The ore deposits are characterized and Sub-Hercynian and Laramian deformations, late related to the metallogenic units of different rank, Maastrichtian–Eocene collision and post-collision- based on the metallogenic analysis of existing pub- al orogeny in the evolution of the Balkan System lished and National Geological Fund data. (Boyanov et al., 1989; Dabovski et al., 1991, 2002; Popov, 1996, 2002; Dabovski, Zagorcev, 2009). The late Maastrichtian–Eocene collision is marked Tectono-magmatic characteristics by foredeep in the Balkanides, isolated continental basins to the south and granitoid magmatism in the The late collisional stage in the Alpine-Balkan Oro Morava-Rhodope Zone and the subsequent Illyrian genic System evolution is characterized by tangen- compression. The Rila-Rhodope Metallogenic Zone, tial compression, which commence by the end of the with specific mineralization, is formed in relation to Late Cretaceous (Maastrichtian) and terminates in the magmatism. The purpose of this study is to dif- the middle Eocene (Lutetian). The collision is char- ferentiate the mentioned magmatism in the Balkan acterized by formation of fold-thrust structures in evolution and to focus on the associated ore depos- association with the granitoid magmatism, specific its and occurrеnces for the ore potential prognosis sedimentation and high-grade metamorphism. The

56 sedimentation is marked by the rhythmic molasses plutons are exposed in the southern parts of West- in the Kula-Obzor Foredeep, as well as by the conti- ern Rhodopes and they are composed of porphyroid nental deposits in the Eastern and Central Rhodopes and aplitoid granite (Kozhoukharov et al., 1963f1; Mts, Eastern Stara Planina Mt., the strip between Soldatos et al., 2008; Dabovski et al., 2009). The the towns of Kazanlak and Burgas, Panagyurishte Yugovo pluton extends in the northern parts of the and Central Stara Planina Mt. (Juranov, Pimpirev, Central Rhodopes and it is represented by several 1989; Goranov, Atanasov, 1992; Juranov, 1992; bodies, composed of quartz-monzodiorite, granodi- Sinnyovsky, Sultanov, 1994; Kânčev, 1995; An orite and monzogranite (Kožuharova, Kožuharov, gelov et al., 2008, etc.). Simultaneously, a series 1962). Obviously, the Dobralak granodiorite, situat- of Maastrichtian–Lutetian granitoid plutons are in- ed NW from the village of Narechenski Bani is also truded in the southern area of the Balkan Orogenic a part of the same group (Kožuharova, Kožuharov, System, in part of the Morava-Rhodope Zone, 1962). The small Topolovo granodiorite pluton is within the Rila and Rhodopes. Thus, a collisional defined to the South from the town of Asenovgrad magmatic arc originated from the hinterland mar- (Marchev et al., 2013). Numerous small stock-like gins. Fragments of the basement in the area are rep- and dyke-like granite bodies are exposed in the resented by rocks of polyphase regional amphibolite northern parts of the Rhodopes, in the areas of the facies metamorphism, which is manifested in rela- towns of Velingrad, Batak and Mihalkovo, and they tion to the Neoproterozoic, Caledonian, Hercynian, should be included in the Maastrichtian–middle Eo- Cimmerian, Austrian, Illyrian and Pyrenean pro- cene magmatic complex. The Smilyan pluton, com- cesses (Jaranoff, 1960; Kozhoukharov et al., 1988; posed of leucocrate to aplitoid granite and located to Boyanov et al., 1990; Peycheva, von Quadt, 1995; the South from the town of Smolyan, is also related Peycheva et al., 1993, 2000, 2004, 2007; Burg et to this complex (Kozhoukharov et al., 1992; Rae- al., 1996; Ivanov, 2000; Ivanov et al., 2000; Liati, va et al., 2006; Kaiser-Rohrmeir et al., 2013). The Gebauer, 2001; Cherneva et al., 2002; Ovcharova small Pripek, Drangovo and Dolen plutons in the et al., 2002, 2003a, b; Arkadakskyi et al., 2003; area of the town of Zlatograd are composed of gran- Carrigan et al., 2003; Ichev, Pristavova, 2004; von ite with transition to granodiorite, quartz-diorite and Quadt et al., 2006, 2008; Bonev, 2006; Zagorchev, quartz-monzodiorite (Kozhoukharov et al., 1995). 2008; Sarov et al., 2008a, b; Dabovski et al., 2009; The Chuchuliga and Rozino granite plutons and nu- Bonev et al., 2010; Bonev, Stamfli, 2011; Zagorchev merous smaller bodies are exposed in the Eastern еt al., 2011, 2015a, b; Kunov et al., 2012; Antić et Rhodopes, between the towns of Krumovgrad and al., 2015, etc.). Particularly Bonev (2006) noted Ivaylovgrad (Belmustakova et al., 1995; Stoykov, Late Cretaceous–Paleocene contractional dome and Mavroudchiev, 1997; Marchev et al., 2006). thrust deformations, which are followed by exten- These plutonic rocks, formerly described as sion and exhumation after the middle Eocene. The “South-Bulgarian granite”, are presumed as Ar- noted Post-Austrian compressional processes in the chean (Bonchev, 1928), Caledonian (Dimitrov, Balkan system are marked by north-vergent Sub- 1959), and most often as Hercynian (Dimitroff, Hercynian, Laramian and by notably determina- 1946; Boyadjiev, 1959; Bojadžiev, 1963) as they tive Lutetian Illyrian intensive folding and thrust- are noted on the 1:100000 scale geological map nappe deformations (Jaranoff, 1960; Bončev, 1971, of Bulgaria. Later on, the individual bodies are 1986; Gočev et al., 1970; Yovchev, 1971; Ivanov, dated as Late Cretaceous or Paleogene (Boyadjiev, 1989; Zagorchev, 1995, 2014; Tzankov et al., 1995; 1959, 1971; Kožuharova, Kožuharov, 1962; Kos- Dabovski, Savov, 1995; Ivanov, 2000; Nachev, tov, 1963; Boyadjiev, Lilov, 1976a, b; Firsov, 1975; Nachev, 2003; Dabovski et al., 2009; Popov et al., Arnaudov, 1979; Arnaudov, Lilov, 1983; Arnaudov 2012, etc.). et al., 1989; Zagorčev, Moorbath, 1983; Zagorčev The Maastrichtian–Lutetian intrusive rocks from et al., 1987, 1989; Palshin et al., 1974; Valkov et the collisional magmatic arc form Rila-Rhodope al., 1989). The more recent specialized studies, granitoid complex, as the latter is widespread in the mainly by U-Pb zircon method (Table 1), deter- larger part of Rila and Rhodopes Mts (Dabovski et mined that all of the described plutons are formed al., 2009). The largest unit of this complex is the Ri- within the interval of 70–42 Ma (Maastrichtian– la-Western Rhodope batholith, formed consecutive- Lutetian) (Kamenov et al., 1999; Nedialkov et al., ly by granodiorite, granite, leucogranite and aplitoid 1998a; Ovcharova et al., 2003b; von Quadt, Peytch- granite, as individual plutons are differentiated with- eva, 2005; Marchev et al., 2006, 2013; Raeva et al., in it (Valkov et al., 1989; Kamenov et al., 1999; von Quadt, Peytcheva, 2005; Peytcheva et al., 2007). The Spanchevo pluton is included in the complex 1 Kozhukharov, D., N. Katskov, V. Sirkatova, D. Doychev, L. to the west, in Pirin Mt. (Jahn-Awe et al., 2010). Ratiev, V. Stoychev. 1963f. Report on the Geology along the Vucha River Valley. Geological Mapping at a Scale 1:25000. National The Barutin-Buynovo-Elatiya and Dolno Dryanovo Geological Fund, report ІV-0146 (in Bulgarian).

57 Table 1 Absolute ages of the Maastrichtian–Lutetian plutonic rocks from the Rila-Rhodope Complex Таблица 1 Възраст на мастрихт-лютеските плутонични скали от Рило-Родопския комплекс

Pluton Composition Age (Ma) Method Authors granodiorite 69.26±0.26 Rila-Western Rhodope U-Pb zircon von Quadt, Peytcheva, 2005 granite 66.79±0.29 Spanchevo granite 56±0.50 U-Pb zircon Jahn-Awe et al., 2010 Dolno Dryanovo granite 55±0.50 U-Pb zircon Jahn-Awe et al., 2010 55.93±0.28 U-Pb zircon Barutin-Elatiya granodiorite Soldatos et al., 2008 49.99±0.88 40Ar/39Ar biotite 42.22±0.08 U-Pb zircon Kaiser-Rohrmeir et al., 2013 Yugovo granite 51.8 K-Ar Nedialkov et al., 1998b Topolovo granodiorite 52.54±0.19 U-Pb zircon Marchev et al., 2013 Smilyan granite 41.99±0.22 U-Pb zircon Kaiser-Rohrmeir et al., 2013 54.4±0.2 U-Pb zircon Jahn-Awe et al., 2012 Pripek granite 52.8±0.89 U-Pb zircon Ovcharova et al., 2003a Drangovo granite 49.9±0.21 U-Pb zircon Marchev et al., 2013 Dolen granite 42 U-Pb zircon Ovcharova et al., 2003a Chuchuliga granite 68.94±0.40 U-Pb zircon Marchev et al., 2006 Rozino granite 68±15 U-Pb zircon Marchev et al., 2006

2006; Soldatos et al., 2008; Jahn-Awe et al. 2010, 2013; Soldatos et al., 2008; Jahn-Awe et al., 2010, 2013, etc.). Similar younger plutons are found in 2012, etc.). The published data about the petrologi- Pirin, Osogovo, etc., but they are not subject of this cal and geochemical features of these rocks display paper. that they are calc-alcaline to high-K calc-alcaline. The Rila-Rhodope granitoid complex is trans- The 87Sr/86Sr ratio (0.7064–0.7066) shows that they gressively covered at numerous places by proven are formed by mantle-crustal magma with predomi- continental Bartonian–Oligocene sediments and nantly crustal matter with the involvement of the volcanic rocks and associated subvolcanic and metamorphic rocks from the basement (d’Amico et hypabyssal bodies. These relationships are docu- al., 1990; Kamenov et al., 1999; Christofides et al., mented in the areas near Rila-Western Rhodope, 2007; Soldatos, et al., 2008; Dabovski et al., 2009; Barutin-Elatiya, Smilyan, Chuchuliga and Rozino Jahn-Awe et al., 2010, 2012, etc.). The lead isotopes plutons and are noted by all authors and mapped data (208Pb/204Pb vs. 208Pb/204Pb) display that the on the 1:100000 and 1:50000 scale geological rocks originate from the orogenic magma (Amov et maps (Kozhoukharov, 1965; Bahneva, Stefanov, al., 1985; Amov, Valkova, 1994; Amov, Arnaudov, 1975; Bahneva, 1983; Dimitrova, Katzkov, 1990; 2000). It should be mentioned that the geochemi- Kozhoukharov et al., 1992, 1993; Goranov et al., cal data are contradictory and mark subductional, 1995; Sarov et al., 2008a, b, etc.). These data cer- pre-collisional and post-collisional settings, respec- tainly mark the upper age limit of the mentioned tively. This indicates that in the magma genesis pro- plutons. cesses have been involved rocks in different type of The composition of the individual plutons shows tectonic setting and age. that they are mainly composed of granite and grano- Based on the Alpine evolution in the Balkan re- diorite, rarely leucogranite, tonalite and quartz-dior- gion Popov (1996, 2002) assumed that the tectono- ite, and in Yugovo pluton – of quartz-monzodiorite, magmatic events during the Maastrichtian–Lutetian granodiorite and monzogranite (Boyadjiev, 1960, are manifestation of late collisional stage. The in- 1971, 1993; Bojadžiev, 1963; Vergilov et al., 1961; truding of the plutons from Rila-Rhodope granitoid Dabovski, 1968; Dimitrova, Belmustakova, 1986; complex and accompanying sediments are referred Valkov et al., 1989; Kozhukharov et al., 1992; Bel- to as occurrance of the collisional processes. Re- mustakova et al., 1995; Stoykov, Mavroudcheiv, cently, Menant et al. (2016) noted the presence of 1997; Nedialkov et al., 1998a, b; Kamenov et al., continental accretion in these areas, with an approx- 1999; Ovcharova et al., 2003a; Marchev et al., 2006, imately in the same age range (65–35 Ma). Other

58 authors, argued the examined plutons as a result of places (absarokite, shoshonite, latite, trachyte, mon- extensional (Ivanov, 1989, 2000), early extension- zogabbro, monzodiorite, quartz-monzonite, etc.). al (Georgiev, 2012) or post-collisional processes The age of the rocks is determined by the relation- (Marchev et al., 2013). The conceptions of these au- ships with the sediment formations and by K-Ar, thors are unconvincing, regardless of the extension- 40Ar/39Ar, U-Pb and Rb-Sr studies (Ivanov, 1960; al manifestations in individual locations of struc- Ivanov, Černjavska, 1971; Bahneva, Stefanov, tural deformations or magma intrusions. Dabovski 1975; Petković, 1981; Bahneva, 1983; Vatsev, et al. (2009) regarded the Late Cretaceous–Tertiary 1984; Zagorčev et al., 1987; Kolocotroni, Dixon, time as extension and exhumation period (unlike 1991; Peczkay et al., 1991; Kozhoukharov et al., Dabovski et al., 1991), but the data show that these 1993; Goranov et. al., 1995; Boyanov et al., 1995; processes started in the middle Eocene. The charac- Eleftheriadis, 1995; Harkovska et al., 1998, 2003, ter and the sequence of the geological events in the 2010; Yanev, 1998; Yanev et al., 1998a, b; Milo- Alpine determine the collisional conditions of the vanov et al., 2005; Georgiev, Milovanov, 2006; Maastrichtian–Lutetian tectonic environment. As it Marchev, 2006; Raeva et al., 2006; Peytcheva et al., was mentioned, the Late Cretaceous in the region is 2007, 2012; Jahn-Awe et al., 2010, 2012; Georgiev marked by basic-intermediate mantle-crustal, high- et al., 2012, etc.). K calc-alkaline and transition alkaline magmatism, The peculiarities in the metallogenic specializa- associated with deep-water, predominantly flysch- tion of the described Maastrichtian–Lutetian mag- like sedimentation, with concomitant Sub-Hercyni- matic rocks in the Rhodopes and Rila Mountains an and subsequent Laramian deformations (Bončev, in comparison to the other ore-magmatic systems 1966, 1971, 1986; Popov, 1981, 1987; Dabovski, in the region should be noted. The earlier Sredno- Savov, 1995; Zagorchev, 1995; Zagorchev et al., gorie Late Cretaceous magmatism, which is deep, 2001; Dabovski et al., 2002, 2009; Boyanov et al., mantle-crustal, with increased alkalinity, is charac- 2003; von Quadt, Peytcheva, 2005; Georgiev et al., terized with Cu deposits (copper sulphide, porphyry 2012). The Maastrichtian–Lutetian stage is deter- copper, vein type) and subordinate amounts of Fe, mined by the characteristics of the magmatism, sed- Au, Mo and other ores. The Maastrichtian–Lutetian imentation and tectonic deformations. The plutonic granitoids are predominantly crustal, hypabyssal to magmatism, as it was mentioned, is orogenic type, mesoabyssal and orogenic type deposits of U, W, granitoid, predominantly crustal. The sedimentation Mo, Sb, fluorite, and others, associated with them. is marked by the marine molasse in the Kula-Obzor On the other hand, the Bartonian–Neogene post- Foredeep to the North and by the continental sedi- collisional magmatism in the Rhodopes and Rila ments in Sredna Gora and Rhodopes Mountains to Mts is represented by complex of volcanic and less- the South. The stage terminated with the Illyrian de- er hypabyssal, predominantly calc-alkaline to tran- formations, which are marked in the Balkanides and sition-alkaline rocks, which control the formation of in certain areas in Sredna Gora Mountain. numerous Pb-Zn and markedly fewer U and fluorite The post-collisional (Bartonian–Neogene) stage deposits and other insignificant mineralizations. is characterized by sediments and magmatic rocks The presented brief notes show a set of geo- formed in extensional conditions. The present-day logical facts, characterizing the time after the Early orogeny was set up with the forming of a system Cretaceous Austrian events, without being able to of horsts and superimposed depressions or grabens, mention the research works of all authors. It is em- filled with predominantly continental, partly shallow phasised that the Maastrichtian–Lutetian processes marine, mainly terrigenous molasse deposits (Ka- occurred between the Turonian Sub-Hercynian and menov, 1959; Jaranoff, 1960; Bončev, 1966, 1971; Maastrichtian Laramian phases and the Lutetian Il- Yovchev, 1971; Moskovski, 1971; Stoyanov et al., lyrian deformation, respectively. During this time 1974; Kamenov, Panov, 1976; Tashev et al., 1977; interval, between the Moesian Platform and the Vatsev, 1978, 1979; Kojumdgieva, Dragomanov, Vardar suture, is situated the Kula-Obzor Molasse 1979; Dragomanov et al., 1980; Kojumdgieva et al., Foredeep and orogeny, sporadic continental depo- 1984; Nedjalkov et al., 1988; Boyanov et al., 1989; sitions, and predominantly granitoid plutonism. Zagorčev et al., 1989; Zagorchev, 1994; Boyanov, Obviously, this continental accretion environment Goranov, 2001; Popov, 1996, 2002; Dabovski et defines a collisional stage in the evolution of the Al- al., 2002; Popov et al., 2015, etc.). The magmatic pides. The subsequent Bartonian–Neogene events processes are synchronous with the sedimentation, are apparently accomplished in the extensional re- as predominantly calc-alkaline to high-K calc-alka- gime. Continental sedimentation and volcanism, line types of volcanic, subvolcanic and hypabyssal overlaying variegated basement, including the ex- plutonic and dyke rocks are formed (dacite, latite, humed parts of the Maastrichtian–Lutetian plutons rhyolite, trachyrhyolite, granite, granodiorite, etc.). occurred during this time at differentiated fault Transition-alkaline rocks are presented at certain movements.

59 Metallogenic characteristic and fluorite metallogenic specialization. These ore manifestations are clearly different from the known The metallogenic processes, related to the Maast Priabonian–Neogene predominantly Pb-Zn deposits richtian–Lutetian granitoid plutons, are marked in this region. In the past, these mineralizations were by a series of mineral deposits and ore occur- associated with the late Eocene–Miocene volcanism rences, defined within the frame of well deter- in the Rhodope Zone, as some authors considered mined Rila-Rhodope Metallogenic Zone (Fig. 2), them as older (Janischevsky, 1937; Kostov, 1942, which has been till now included in the Rhodope 1943, 1946, 1963; Petrascheck, 1942; Dimitrov, Zone (Bogdanov, 1976, etc.) mainly with younger Tz., 1945; Dimitrov, S., 1959; Dimitrov, R., 1979, polymetallic ores. It is characterized by W, Mo, U etc.). Later on, Dimitrov et al. (1984), Kolkovski

Fig. 2. Map of the Rila-Rhodope Metallogenic Zone 1, Bartonian–Quaternary cover; 2, Maastrichtian–Lutetian granitoid rocks; 3, Paleocene–Lutetian sediments; 4, Mesozoic basement; 5, Paleozoic–Neoproterozoic basement; 6, Rila-Rhodope Metallogenic Zone (RRZ); 7, оre regions (Rila-Western Rhodope (RWR), Rakitovo-Bachkovo (RB), Barutin-Smilyan (BSM)); 8, ore fields and mineralized areas (a, Grancharitsa; b, Babyak; c, Beli Iskar; d, Beslet; e, Ribnovo; f, Belovo; g, Srebren; h, Yugovo-Narechen; I, Mihalkovo; j, Batak; k, Dolno Dryanovo; l, Barutin; m, Smilyan); ore deposits: 9–10, skarn (9, iron; 10, copper); 11–21, hydrothermal (11, molybdenum; 12, molybdenum-tungsten; 13, tungsten; 14, copper; 15, lead-zinc; 16, polymetallic; 17, gold-lead-zinc; 18, gold-polymetallic; 19, gold-silver; 20, uranium; 21, gold-antimony); 22, antimony; 23, fluorite stratiform; 24, uranium infiltrational Фиг. 2. Карта на Рило-Родопската металогенна зона 1 – бартон-кватернерна покривка; 2 – мастрихт-лютески гранитоидни скали; 3 – палеоцен-лютески седименти; 4 – ме- зозойска подложка; 5 – палеозой-неопротерозойски фундамент; 6 – Рило-Родопска металогенна зона (RRZ); 7 – рудни райони (Рило-Западнородопски (RWR), Ракитово-Бачковски (RB), Барутин-Смилянски (BSM)); 8 – рудни полета и ми- нерализирани площи (а – Грънчаришко, b – Бабяшко, c – Белоискърско, d – Беслетско, e – Рибновско, f – Беловско, g – Сребренско, h – Югово-Нареченско, i – Михалковско, j – Баташко, k – Долнодряновско, l – Барутинско, m – Смилянско); рудни находища: 9–10 скарнови (9 – железни; 10 – медни); 11–21 хидротермални (11 – молибденови; 12 – молибден-волф рамови; 13 – волфрамови; 14 – медни; 15 – оловно-цинкови; 16 – полиметални; 17 – злато-оловно-цинкови; 18 – злато-по- лиметални; 19 – златно-сребърни; 20 – уранови; 21 – злато-антимонови); 22 – антимонови; 23 – флуоритови стратиформ- ни; 24 – уранови инфилтрационни

60 (1989), Maneva et al. (1994), Popov (1996, 2002), ores. Metasomatic alterations as greizenization (Ba Maneva (1997), Kolkovski and Georgiev (2006), byak, Grancharitsa, Srebren, Smilyan), zeolitization Georgiev et al. (2007) confirmed the differen- (Beli Iskar), jasperoidization (Mihalkovo, Ribnovo), tiation of the examined ore deposits as one Late etc., are characteristic for many of the ore manifes- Cretaceous–early Tertiary metallogenic unit, nomi tations, but are not typical for the upper Eocene–Ol- nated by Popov (2002) as Pirin-Rhodope Metallo igocene mineralizations. Besides the skarn deposits, genic Zone and by Kolkovski and Georgiev (2006) the age of the Ribnovo Sb deposit is unquestion- as Western Rhodope complex dome (including Rila able, as it is formed within the granitoids and cov- and Pirin Mts). The cited age data for the plutons ered by the upper Eocene–Oligocene sediments and from Rila-Rhodope granitoid complex clearly mark volcanogenic rocks. It should be mentioned the age the Maastrichtian–Lutetian Rila-Rhodope Metal determinations of individual deposits by Amov and logenic Zone. Valkova (1994), based on model parameter of the The Rila-Rhodope Metallogenic Zone is defined thorogenic lead 208Pb/204Pb, as well as the pegmatite by complex of post-magmatic pegmatite, skarn and dating by U-Pb zircon method by Arnaudov et al. hydrothermal ore deposits and occurrences. The (1990) (Table 2). Of course, these determinations pegmatites are formed at the earliest stage and some are approximate. Unfortunately, there are currently occurrances are economically significant for feld- no data from more accurate and modern radiogenic spar or muscovite production such as Velingrad, age determination methods. Kalin, Dolno Osenovo, Vishteritsa, Popova Glava, Selishte, etc. (Ivanov, 1989). The skarn ores are characterized by Fe ore occurrences (Golak, Kru- Table 2 shevo, Mihalkovo, Lyaskovo, Kostandovo, etc.). Absolute ages of the ore deposits from the Rila-Rhodope They have a limited economic value but some of Metallogenic Zone based on thorogenic lead, 208Pb/204Pb their parts were exploited in antiquity. The W, Mo, values (Amov, Valkova, 1994), and for pegmatite – by U and fluorite post-magmatic hydrothermal ores U-Pb zircon method (Arnaudov et al., 1990) predominate in the considered metallogenic zone. Таблица 2 Bismuth, Sb and Au are found in lesser amounts, Възраст на рудните находища от Рило-Родопска while Pb, Zn and Cu are rare. Uranium, W, Mo, Mo- металогенна зона въз основа на торогенно олово, 208 204 W, Mo-fluorite, Au-Mo, W-Mo, W-Bi, W-Mo-Bi, по стойностите на Pb/ Pb (Amov, Valkova, 1994), а пегматитите – по U-Pb на циркони (Arnaudov et al., fluorite, Sb, Au-bearing Sb, Au-Ag, Bi, rare Pb-Zn, 1990) Au-Pb-Zn and Cu ores are differentiated in accord- ance with the presence of ore components in the in- Deposits Age (Ma) dividual deposits. Several U (Beli Iskar, Beslet) and Pegmatites 58–48 fluorite (Mihalkovo) deposits are of economical Babyak 80±15 value and have been recently mined. Besides, Gran- Skrebatno 80±10 charitsa W, Babyak Au-Mo, and some other depos- Mehovtsi 55±5 its (Yugovo, Ribnovo, etc.) are considered to be of Tsrancha 60±20 economical value as well. The geological-structural Removo, Tsvetino 55±15 features and the mineral composition are studied Yugovo 75±15 in the individual deposits. With some exceptions, Mihalkovo – Gagovi Nivi 80±5 complete modern specialized mineralogical-geochemical studies are not performed to validate their genetic characteristics. Revealing the relationships between the men- The metallogenic processes, related to the evo- tioned ore mineralizations and the Upper Creta- lution of Maastrichtian–Lutetian plutons, determine ceous–middle Eocene granitoids is one of the main the formation and location of the separate ore-bear- problems. The analysis shows that these relation- ing units. The spatial distribution of these plutons ships are proved mainly by field geological corre- defines the spreading of the Rila-Rhodope Metal- lations with the host rocks and their mineralogical logenic Zone. The Rila-Western Rhodope, Rakito- features, as the individual ore manifestations are vo-Bachkovo and Barutin-Smilyan ore regions are described below. At first place are mentioned the divided within this zone. Separate ore fields or min- pegmatite deposits, related to the granitoid plutons, eralized areas are outlined within the individual ore as well as the skarn Fe manifestations along their regions. contacts. The hydrothermal ore mineralizations are The Rila-Western Rhodopes Ore Region in- formed within the frames of the granitoid bodies or cludes Rila and NW part of Rhodopes Mountains, their exocontacts. Practically they are not observed as it is defined by the spatial extent of Rila-West- together with the upper Eocene–Oligocene Pb-Zn ern Rhodope batholith. The geological exploration

61 somatic processes are represented by chloritization, epidotization, sericitization and silicification. The individual ore veins are 100–400 m long and 0.3– 25 m thick, with halo of disseminated mineralization. Scheelite is the main ore mineral and high content of quartz and pyrite is typical. Cassiterite, tungstenite, magnetite, arsenopyrite, hematite, bismuth- ine, molybdenite, sphalerite, galena, chalcopyrite, Fig. 3. Geological cross-section across the Grancharitsa marcasite, chlorite, fluorite, heulandite, etc., are tungsten deposit (after Mirchev, 1995f) found as well (Egel et al., 1978; Mirchev, 1995f). 1, Western Rhodope granite; 2, Grancharitsa granodiorite; 3, The W ore occurrences (Manashitsa, Krastava- Babyak-Grashevo dislocation; 4, ore hosting faults (1, main ore zone; 2, ore zone No 2; 3, Grancharitsa-South zone; 4, Transko West, Kavunova Mogila) are located in ENE or NW Dere; 5, Planinsko Dere); 5, scheelite mineralization halo fault zones with greizenization and to a lesser extent zeolitization, epidotization and pyritization of the Фиг. 3. Геоложки разрез през волфрамовото находище Грънчарица (по Mirchev, 1995f) rocks. The ore minerals are represented by pyrite, 1 – Западнородопски гранити; 2 – Грънчаришки гранодио scheelite and hubnerite, rarely bismuthinite, Pb-Bi рити; 3 – Бабяшко-Грашовска дислокация; 4 – рудонос- sulfosalts, chalcopyrite, bornite, malachite, fluorite, ни разломи (1 – основна рудна зона, 2 – рудна зона № 2, etc. (Klimov et al., 1991f3; Mirchev, 1993f4). 3 – зона Грънчарица-юг, 4 – Трънско дере, 5 – Планинско The Pb-Zn ore occurrences (Tsvetino, Kalyata, дере); 5 – ореоли от шеелитова минерализация Mehovtsi) are located in longitudinal and latitudi- nal faults, along with silicification, greisenization, chloritization, kaolinization, etc. They are repre- works in this ore region outline the Beli Iskar, Bab- sented by ore veins with galena, sphalerite, pyrite and less chalcopyrite, arsenopyrite, etc. (Mirchev, yak, Grancharitsa, Beslet, Srebren and Ribnovo ore 5 fields and the Belovo mineralized area (Fig. 2). 1993f, 1995f; Vasilev, Endyakov, 1985f ). The Grancharitsa Ore Field is located 12–23 km The Bi Alan Dere ore occurrence is represented SW of the town of Velingrad. It is developed in part by longitudinal faults with mineralization of bis- of the Rila-Western Rhodope batholith, including muthinite associated with pyrite, hematite, magnet- within the late vein fine-grained granite. The ore ite, sphalerite, and galena (Mirchev, 1993f). is formed underneath the Babyak-Grashevo fault, The Babyak Ore Field is located SSE from the which is sub-equatorial with moderate dip to the town of Yakoruda, where the Maastrichtian–Lute- North. The ore field is characterized by the Gran- tian granitoids and high grade metamorphic rocks charitsa W deposit and the Manashitsa, Krastava- are exposed. The Babyak-Grashevo fault is ore con- West, Kavunova Mogila W, the Grashovo Mo-W, trolling and ore hosting and represents a series of the Tsvetino, Mehovtsi and Kalyata Pb-Zn, Alan smaller NNW, sub-meridional and NE structures, Dere Bi, Avramovi Kolibi, St. Petka Cu and other formed in the main fault hanging wall. The meta- ore occurrences (Egel et al., 1978; Mirchev, 1995f2). somatic alterations similar to greisenization are The Grancharitsa deposit is at 18 km SW of the typical (sericite, muscovite, fluorite, calcite, beryl, town of Velingrad. It is formed underneath the Ba- apatite, quartz, microcline, etc.). The ore field is byak-Grashevo dislocation, dipping 10–15° to the characterized mainly by the Babyak Mo (Ag- and North (Boyadjiev, 1971; Katzkov, Marinova, 1992), Au-bearing) deposit. Furthermore, the Chilikovo where a series of ore veins in subparallel faults are recorded. The main ore zone is 8 km long and being more than 1600 m in depth. It has complicated 3 Klimov, I., P. Nikolov, R. Dimitrova, K. Miloshev, S. Milev, P. Petrov, M. Petrova. 1991f. Report on the Results from the Prospecting structure, with smooth bends along the strike and dip and Estimating Implemented in Rare Metal Mineralizations in Part and with numerous apophyses (Fig. 3), as separate from Western Rhodopes, Specialized Geological Mapping at a Scale sectors are differentiated. Several smaller ore zones 1:10 000 Implemented in the Area between Babyak, Krastava and Eleshnitsa Villages. National Geological Fund, report ІV-0383 (in (Grancharitsa-South, Tralsko Dere, Vezov Dol and Bulgarian). Planinsko Dere) are documented below the main 4 Mirchev, N. 1993f. Report on the Detail Prospecting Imple zone. The ore hosting faults are sub-equatorial, dip- mented in Western Rhodopes Area on Manashitsa, Babayak-East, ping at 10–50° to the North. The hydrothermal meta- Yurukovo Tungsten Ore Occurrences, Alan Dere Bismuth Ore Occurrence, Pisani Skali Gold-Silver Ore Occurrence and the Perspectives About the Ore Deposits Presence in the Area of Gran charitsa-Babyak Ore Field. National Geological Fund, report І-1125 2 Mirchev, N. 1995f. Report on the Final Results from the Geo- (in Bulgarian). logical Exploration Implemented in the Grancharitsa Tungsten Deposit 5 Vasilev, V., D. Endyakov. 1985f. Report on the Results from and the Adjoining Tralsko Dere, Vezov Dol, Tsarnyaka, Grancharitsa- the Detailed Prospecting Implemented in Mehovtsi Lead-Zinc Ore South and Zone No 2 Ore Occurrences. National Geological Fund, re- Occurrence, Blagoevgrad District. National Geological Fund, report port І-1232 (in Bulgarian). І-1025 (in Bulgarian).

62 submeridional faults in the gneiss and granite. Six ore veins with economic value are recorded as the biggest one reaches 1250 m in length and is 0.3– 8 m thick. The Mo is the main metal with economic value and Bi, Ag and Au are of secondary importance. Pyrite and molybdenite are the main ore minerals, sphalerite, bismuthinite and galena are lesser, and chalcopyrite, magnetite, cassiterite, tungstenite, scheelite, arsenopyrite, native gold, aikinite, ko- salite, lillianite, and tennantite are rare. The quartz is the most widespread gangue mineral, as microcline, sericite, fluorite, chlorite, calcite, barite, and zeolites are represented as well (Ekimov, 1978f; Egel et al., 1978). The Babyak-East tungsten ore occurrence is located east of the homonymous village. Complicated 1.1 km long fault zone, with 290–300° direction and 45–89° dip to NNW, is traced in the Maastrich- tian–middle Eocene granite. Feldspatization, greisenization, quartzitization, sericitization, and weak albitization are determined in the zone. The ore mineralization is developed in the brecciated metasomatic rocks. Hubnerite and scheelite are the main ore minerals; pyrite, aikinite, bismuthinite, and molybdenite are subordinate. The gangue minerals are represented mainly by quartz and lesser amounts of feldspar, mica, and fluorite. The discovered secondary minerals are stolcite, chalcocite, covellite, and

ferrous hydroxides. The ore contains mainly WO3 Fig. 4. Geological map of the Babyak molybdenum (silver and lesser amounts Mo, Bi, Pb, Zn, Cu, Ag, and Au and gold bearing) deposit (after Ekimov, 1978f) (Klimov et al., 1991f; Mirchev, 1993f). 1, Western Rhodope Upper Cretaceous–middle Eocene gran- The Dagonovo tungsten ore occurrence is lo- ite; 2, marble; 3, gneiss; 4, Babyak-Grashevo dislocation; 5, ore hosting fault cated near the homonymous village. Aplitoid-pegmatite granite and gneiss with marble layers are ex- Фиг. 4. Геоложка карта на молибденовото (сребро- и posed in the area. Along the contact between these златосъдържащо) находище Бабяк (по Ekimov, 1978f) 1 – Западнородопски горнокредно-средноеоценски грани- rocks 30–45 m thick fault zone with 150–170° di- ти; 2 – мрамори; 3 – гнайси; 4 – Бабяшко-Грашовска дисло- rection is formed. The rocks are chloritized, kao- кация; 5 – рудоносни разломи linized, silicified; the marbles are skarned. The ore minerals are scheelite, calcite, fluorite, and smaller amounts of pyrite, chalcopyrite. The secondary minerals are malachite, azurite, Mn and Fe hydrox- Blato Mo, Babyak-East and Dagonovo W, Yuruk- ides (Kostov et al., 1984f7). ovo and Gabnika W-Bi, Zarovets, Chervena Mogila The Yurukovo W-Bi ore occurrence is SE of the and St. Georgi W-Mo-Bi, Lyutak and Shehovtsi homonymous village. Biotite granite, gneiss and polymetallic, Temnitsko and Pisovets Cu ore occur- marble are developed in this area, where a strip of rences and numerous mineral indications are found silicified and skarned rocks 1500 m long and 280– as well (Ekimov, 1978f6; Egel et al., 1978; Vasilev, 500 m wide is traced. Eight vein-like structures Endyakov, 1985f; Klimov et al., 1991f; Mirchev, with W and Bi ores are documented in this zone 1993f, 1995f). (Mirchev, 1993f). The Babyak deposit includes the Duyovi Dupki The Gabnika W-Bi ore occurrence is 1 km NE (Babyak-I) and Kardashovi Kolibi sectors (Fig. 4). of the village of Babyak, where the granite is cut by Series of hydrothermal quartz-Mo veins are developed within the deposit and are localized in the 7 Kostov, I., A. Mladenov, R. Kamilova. 1984f. Report on the Geological Mapping carried out at 1:10 000 Scale with Prospecting and Research of Metasomatic Type Tungsten-Molybdenum-Bismuth 6 Ekimov, G. 1978f. Report on the Results of the Geological Re- Mineralizations in the Lands of Babyak, Yurukovo, Dragonovo search Implemented in Babyak Molybdenum Deposit, Blagoevgrad Villages, Blagoevgrad District. National Geological Fund, report ІV- Area. National Geological Fund, report І-0915 (in Bulgarian). 0347 (in Bulgarian).

63 NW fault zone dipping at 55–70° to SW. The rocks are silicified and greizenized. 0.25–0.80 m thick vein with interrupted mineralization of hubneite and scheelite is recorded (Klimov et al., 1991f). The Zarovets W-Mo-Bi ore occurrence is situated 6 km western from the town of Yakoruda. Gneiss and marble, intersected by granite dykes and aplites are outcropped in the area. A zone of intensive cracking is traced as well. The rocks are altered by K and Si metasomatization and subsequently – by adu- larization, albitization and greizinization and finally – by carbonatization. The ore mineralization is represented by scheelite, molybdenite and bismuthinite in small quartz veins. The pyrite, magnetite, chalcopyrite and sphalerite are rare (Kostov et al., 1984f). The Beli Iskar Ore Field is located in the northern parts of Rila Mountain (Fig. 2). Maastrich- tian–Lutetian granitoid with diorite porphyrite and granite porphyry dykes, pegmatite, aplite and quartz veins and xenoliths of high grade metamorphic rocks are exposed in the area. The ore controlling longitudinal Beli Iskar multiple fault zone is traced from the Rila Monastery, in front of Beli Iskar dam, to the Belmeken Peak. NW, NE and rarely sub-meridional faults are also observed at some places. The U deposits Beli Iskar and Partizanska Polyana, Belmeken ore occurrence and numerous mineral indications are found (Si- mov, 1980; Dimitrova, Katzkov, 1990; Skenderov Fig. 5. Geological cross-section across the Beli Iskar ura- et al., 1994f8). nium deposit (after Simov, 1980) The U ore in Beli Iskar deposit is developed 1, granite; 2, ore hosting fault around one of the faults from the Beli Iskar zone Фиг. 5. Геоложки разрез през урановото находище Бели (Fig. 5). The deposit is located NE from the Beli Искър (по Simov, 1980) Iskar dam. Around the fault are formed series of 1 – гранити; 2 – рудоносни разломи cracks, brecciated and milonitized structures with direction of 65–85° and 70° dip to South, which are probably feathering to the main fault. The ore mineralization is irregularly distributed along the main of the ore hosting fault. Besides, the ore mineraliza- fault and the feathery structures as lenticular and tion is developed below the tectonic clay, below the vein-like ore bodies are developed (Stoykov, 1976; hanging contact of the fault (Stoykov, 1976; Simov, Simov, 1980). 1980). The Partizanska Polyana deposit (at the ho- The Belmeken ore occurrence is in the eastern monymous meadow) is in the western part of the part of the ore field, where sub-equatorial to ENE ore field, along the Manastirska River, near the Rila faults of the Beli Iskar fault zone and smaller sub- Monastery. The ore mineralization is formed in a meridional faults are observed. The ore mineraliza- fault with NW direction (300–310°) and 20–40° tion is hosted in the faults from both directions, as dip to NE (Fig. 6), which is joined to the Beli Iskar it predominates in the ENE faults. The morphology fault zone. The ore body is vein-like, compound by of the ore bodies is diverse (Stoykov, 1976; Simov, quartz, carbonates and zeolites. Thicker tectonic 1980). breccia and higher concentrations of the ore min- The hydrothermal alterations around the faults eralization are documented in the more slant parts are represented predominantly by zeolitization, carbonatization and weak chloritization. The ore mineralization in the deposits is mainly uranophane, 8 Skenderov, G., L. Dragomanov, D. Boykov, V. Darakchiev, I. uranophane-beta, U-bearing fluorapatite, rarely Bedrinov. 1994f. Explanatory Notes to the Legend of the Metallogenic autunite. Iron hydroxides, magnetite, hematite and Map of Uranium at 1:200 000 Scale of the Republic of Bulgaria, individual grains of chalcopyrite are found as well. Petrich Map Sheet. National Geological Fund, report І-1225, 128 p. (in Bulgarian). The gangue minerals are zeolites (stilbite and less

64 the place of Beslet Peak and the village of Medeni Polyani. Granite from the Western Rhodope pluton and small bodies of fine grained biotite granite are mainly outcropped in this area. They are intruded in the high grade metamorphic rocks (gneiss, gneissic schist, schist, rarely marble). Southeastern (110– 140°), northeastern (35–70°) and sub-meridional (350–10°) faults are traced (Katzkov, Marinova, 1992; Vladov et al., 1971f9). Fig. 6. Geological cross-section across the Partizanska Po The U deposits Beslet and Kalach Burun and the lyana uranium deposit (after Stoykov, 1976) ore occurrences Patevoto, Kara Tepe, Kayali Dere, 1, granite; 2, ore body; 3, fault Skrebatni Polyani and others are developed in this Фиг. 6. Геоложки разрез през урановото находище ore field. The U ores are localized along the faults Партизанска поляна (по Stoykov, 1976) in granite, which have different directions in indi- 1 – гранити; 2 – рудни тела; 3 – разломи vidual areas. Two hydrothermal alteration stages are presented in the granite near the faults. The first stage is high temperature, represented by microclin- ization, albitization and greisenization. The second low temperature stage is marked by seritization, silicification and carbonatization. Vein-like greisen rosary-like bodies are outlined around the faults. Greisenized granite is observed in the outer parts of these bodies, and there are quartz-muscovite or quartz-sericite greisens in the inner parts. Quartz- sulfide veinlets with pyrite, arsenopyrite, chalcopyrite, chalcocite, covellite, galena and sphalerite with increased Au and Ag content are found within the greisen bodies (Aladzhov et al., 1984f10). The Beslet deposit is located in the area of the homonymous peak, at about 32 km SW of the town of Velingrad. Faults with direction about 80° and 40–60° dip to south and faults with 350–10° direction and 80–90° dip to east are observed in the area. The U ores are developed in the places of intersec- tion between faults from both directions. The ore bodies are elongated along the faults with direction of 80° (Fig. 7). The Kalach Burun deposit is at 25 km SW from the town of Velingrad. The ore bodies are localized in a fault zone (Fig. 8). The individual faults have directions from 30 to 90°, and the dip varies from 45 to 80° to NW–N. The U mineralization is spatially related to the greisenization, as it is pre- cipitated in the fractured and brecciated zones in Fig. 7. Geological cross-section across the Beslet uranium the greisen rocks. The ore bodies are vein and len- deposit (after Simov, 1980) ticular in shape. From the surface down to depth 1, granite; 2, greisenized zone; 3, ore body of 100–120 m the U mineralization is represented Фиг. 7. Геоложки разрез през урановото находище Бес лет (по Simov, 1980) 1 – гранити; 2 – грайзенизирана зона; 3 – рудни тела 9 Vladov, T., M. Kunchev, H. Krastev, V. Krasteva, K. Petrova, P. Petrov, A. Shopov. 1971f. Report on the Results from the Geologi- cal Exploration and Drilling Implemented along the Dospat Fault in Selishte-Medeni Polyani Area and Beslet Deposit from the Dospat laumonite), carbonates (calcite and rarely arago- Group. National Geological Fund, report ХХІІІ-3842 (in Bulgarian). nite) and quartz (Stoykov, 1976; Simov, 1980). 10 Aladzhov, T., D. Dikov, T. Dimitrov, K. Velkov, M. Zlatkova, S. The Beslet Ore Field is located in the Western Yosifova, I. Piskyulev. 1984f. Intermediate Report of Rhodopes Group for the Specialized Prospecting and Estimation Implemented in Medeni Rhodopes (Fig. 2). It covers part of the southern Polyani-Tsvetino and Chukata Area. National Geological Fund, report area of the Rila-Western Rhodope batholith, in ХХІІІ-4029 (in Bulgarian).

65 The Sb (+Au) Ribnovo deposit is located near the homonymous village. Ancient works are discovered, as small-scale mining production of antimony was done during 19 and first half of 20 century. Si- licification, sericitization, carbonatization and chloritization of the rocks are developed in the tectonic breccia of the Kurtovitsa fault (Vatsev, 1965f12). “Minorco Services” (1998f13) regard the meta- somatism as jasperoidization. The ore is bed-like (Fig. 9), located predominantly in the interbedding fault. Second ore zone is found in the Pre-Oligocene weathering crust, which is compound by clay cap over the hydrothermally alternated rocks. The ore has quite irregular distribution and is concentrated in enriched nests, up to 0.6 m long, with 2–8% Sb content (Vatsev, 1965f, 1987). The antimonite and arsenopyrite are the main ore minerals in the deposit and pyrite, sphalerite, galena, chalcopyrite and Fig. 8. Geological map of the Kalach Burun uranium deposit (after Simov, 1980) marcasite are minor to rare. The gangue minerals 1, granite; 2, greisenized zone; 3, ore body are mainly quartz and to a lesser extent calcite. Hy- droromeite, stibiconite, hydroservantite, kermesite, Фиг. 8. Геоложка карта на урановото находище Калъч бурун (по Simov, 1980) realgar, orpiment, Fe hydroxides and others are ob- 1 – гранити; 2 – грайзенизирана зона; 3 – рудни тела served as secondary minerals (Vatsev, 1965f). The investigation of “Minorco Services” (1998f) shows that the Au grade is low. In the weathering crust the ore body is bed-like and non-economic value. The by autunite, torbernite and rarely zeunerite. Urano- weathering crust sealed the hydrothermal fluids, phane, residues of U minerals and pitchblende (na- as ore mineralization is missing in the Paleogene sturane) are present in depth. Chalcopyrite, sphaler- rocks. ite, galena and gold are also found in depth. Iron and The Sb (+Au) Kremenitsa ore occurrence is Mn hydroxides are observed in the oxidized parts situated 2 km southern of the village of Ribnovo. (Aladzhov et al., 1984f; Stoev et al., 1995f11; Sken- Gneiss, marble and serpentinite are present in the derov et al., 1994f). area and overlaid by Paleogene breccia conglomer- The Ribnovo Ore Field is located in the Western ate. Fault zone with direction of 105–135° and length Rhodopes, 10–20 km NE from the town of Gotse about 1.2 km is traced. The tectonically brecciated Delchev (Fig. 2). The area is composed of a vari- marble is altered to jasperoid. Quartz lenses up to ety of gneiss, to a smaller extent gneissic schist, 2.5 m long and 0.6 m wide are differentiated within amphibolite, marble, etc., as well as granite to the it. The ore minerals are radial antimonite, pyrite, NE. Upper Eocene–Oligocene terrigenous, pyro- marcasite, arsenopyrite and chalcopyrite. The sec- clastic and acid effusive rocks are preserved in cer- ondary minerals are stibiconite, hydroservantite and tain places. The Ribnovo fault strikes to the West Fe hydroxides (Kozhukharov et al., 1958f14). “Mi with direction of 150–170° (Jaranoff, 1960), as norco Services” (1998f) determined high Au con- faults with 110–140° directions, are documented in centrations in some samples only. the ore field. The Kurtovitsa thrust-nappe (Vatsev, 1987) has significant ore-controlling importance. It is interbedding, with 10–30° dip to SW and thickness of 2–15 m. The fault is along the crystallization 12 Vatsev, M. 1965f. Report on the Preliminary and Detail Ex schistosity or the relict bedding between marble and ploration of Antimony Ores from Ribnovo Deposit and Kremenitsa Ore Occurrence and Lead-zinc Ores from Skrebatno Ore Occurrence, gneissic schist. The Sb (+Au) Ribnovo deposit, Kre- Blagoevgrad Area. National Geological Fund, report І-0617 (in menitsa (Osikovo) ore occurrence, Au-polymetallic Bulgarian). Skrebatno ore occurrence and others, are found in 13 Minorco Services. 1998f. Report on the Accomplished Works in the ore field. Belitsa Research Areas. National Geological Fund, report І-1323 (in Bulgarian). 14 Kozhukharov, D., E. Kozhukharova, K. Iliev, P. Paskalev, A. Pencheva, M. Shtereva, T. Paskaleva. 1958f. Report on the Pre- 11 Stoev, L., D. Dekov, L. Dedinski, N. Gospodinov. 1995f. Geo liminary Geological Exploration and Geological Mapping at a Scale logical Note for the Geological Exploration Accomplished in Kalach 1:25 000, Implemented in the Area Southern from the Town of Velin Burun Uranium Ore Occurrence. National Geological Fund, report grad and Rakitovo Village – Western Rhodopes. National Geological І-1223 (in Bulgarian). Fund, report ІV-0056 (in Bulgarian).

66 Fig. 9. Geological cross-section across the Ribnovo antimony deposit (after Vatsev, 1987) 1, Oligocene conglomerate and sandstone; 2, biotite, amphibole-biotite and chlorite-biotite gneiss and gneissic schist; 3, marble; 4, muscovite-biotite and biotite gneiss; 5, weathering crust with noneconomic ore; 6, jasperoid tectonic breccia with arsenic- antimony ore Фиг. 9. Геоложки разрез през антимоновото находище Рибново (по Vatsev, 1987) 1 – олигоценски конгломерати и пясъчници; 2 – биотитови, амфибол-биотитови и хлорит-биотитови гнайси и гнайсо- шисти; 3 – мрамори; 4 – мусковит-биотитови и биотитови гнайси; 5 – изветрителна кора с непромишлено орудяване; 6 – джаспероидизирана тектонска брекча с арсен-антимонова руда

The Au-Pb-Zn Skrebatno ore occurrence is lo- al., 1986f16; Mirchev, 1993f; Kolkovski, Georgiev, cated at the northern edge of the homonymous vil- 2006; Georgiev et al., 2007; Vidinli, 2015; Vidinli, lage. Various kinds of gneisses and some marble are Мladenova, 2016). outcropped. To the west they are overlaid by Paleo- The Au-Ag Srebren (Gyumushchal) deposit is gene terrigenous sediments and tuffs. The Kurto- located at the Srebren Peak ridge area, at 36 km vitsa fault is traced through the metamorphic rocks south from the town of Velingrad and 10 km north (Vatsev, 1965f). The tectonic breccia is enriched from the town of Sarnitsa. It is formed in the Maas- with Fe hydroxides and is covered by Tertiary sedi- trichtian–Lutetian granite with xenoliths of high ments. Sericitization, silicification, carbonatization grade metamorphic rocks. The “Trace Resources” and chloritization are determined within the brec- data (in: Vidinli, 2015) show that the deposit is rep- ciated and cracked metamorphitc rocks. Veinlets, resented by 5 sub-parallel ore zones in one strip, disseminated and rarely small nests with pyrite, which is about 100 m wide, NNE oriented (7–42°) galena, sphalerite, occasionally chalcopyrite are and about 1100 m long (Fig. 10). The ore bodies observed in the ore hosting fault. The Pb and Zn are vein-like, rarely lenticular in shape. Traces from contents are about 0.1%, rarely up to 2% (Vatsev, ancient mining are observed in the oxidation zone. 1965f; Tretyakov, Ivanov, 1953f15). In trenches and The ore has economical grade of Au and Ag and wells “Minorco Services” (1998f) found increased low concentrations of Pb, Zn, Cu, W, etc. The rocks Au contents. in the faults zones are chloritized, sericitized, argil- The Srebren Ore Field includes parts from the lized, silicified, and are assigned by Vidinli (2015) Western Rhodopes, from the village of Gostun to to the quartz-sericitic metasomatites. The carboni- the west, across the Syutka and Srebren Peaks, to zation is rarely observed. The presence of berezites the town of Sarnitsa to the east. Maastrichtian–Lu- (Vidinli, 2015) and greisens (Mirchev, 1993f) is tetian granite and high grade metamorphic rocks noted. are observed in this area. The small Au-Ag Sre- The ore mineralization was studied during the bren deposit and analogous Pisani Skali and Gostun exploration of the deposit (Tretyakov, Ivanov, ore occurrences, W-Bi Sarnitsa-2 ore occurrence 1953f; Angelova et al., 1986f; Mirchev, 1993f) and and smaller mineralizations as Mustalitsa, Cherno later by some specialized investigations by Vidinli Dere, St. Bogoroditsa, Balak Dere, Pilyovitsa, etc. (2015). The pyrite and arsenopyrite are the most are found (Tretyakov, Ivanov, 1953f; Angelova et widespread, followed by sphalerite and galena.

16 Angelova, M., L. Krastev, P. Petrov, N. Yorgova, M. Zhelezanov. 15 Tretyakov, G., I. Ivanov. 1953f. Report on the Results from Pros- 1986f. Report on the Geological Exploration Implemented During pecting and Revision Implemented in Western Rhodopes and Pirin 1955-1978 on Srebren Gold-Silver Deposit, Southern from Velingrad, Mountain Massif Foothill. National Geological Fund, report І-0313 (in Pazardzhik District. National Geological Fund, report І-1032 (in Bul- Russian). garian).

67 60°) are traced, and 4 mineralized zones are found in the faults. The biggest zone (No 1) reaches length of 3 km and thickness of 10–40 m. Ancient mining works have been discovered. The ore bodies are represented by linear stockworks. The hydrothermal alterations are analogous to the Srebren deposit, although more intensive hematitization is noted (Vidinli, 2015). The ore mineralization is represented mainly by pyrite and to a lesser extent hematite and scheelite. Sphalerite, galena, native gold, chalcopyrite, arsenopyrite and ilmenite are of secondary importance and the magnetite, pyrrhotite, cosalite, rutile, lillianite, etc., are rarer (Vidinli, 2015; Vidinli, Mladenova, 2016). The Au followed by Ag are of key importance. The Pb and Zn contents are ~10%, and the W, Mo, Bi and Sn contents are thousandth or ten thousandth of a percent (Mirchev, 1993f). The gangue minerals are represented mainly by quartz and to a lesser extent of sericite, muscovite, chlorite, etc. The supregene minerals are jarosite, cerussite and malachite. Pitchblende (nasturane), torbernite and autunite are also found and are related to the nearby Kalach Burun U deposit. The W-Bi Sarnitsa-2 ore occurrence is located north from the Sarnitsa town. Metamorphic rocks with quartz veins in ESE faults are exposed in the area. Iron hydroxides are observed and the analyses show increased contents of W, Bi, Ag and little Pb, Zn and Cu (Valkov et al., 1972f17). The Belovo mineralized area covers the NE Fig. 10. Geological map of the Srebren gold-silver deposit slopes of Rila Mountain and parts of Ihtiman Sred- (after “Trace Resources”, in: Vidinli, 2015) 1, Maastrichtian–Lutetian granitoid; 2, ore vein na Gora Mountain, where the towns of Kostenets and Belovo are situated (Fig. 2). Gneiss, gneissic Фиг. 10. Геоложка карта на златно-сребърното находи- schist, marble, amphibolite are outcropped and the ще Сребрен (по “Трейс Рисорсиз”, във Vidinli, 2015) 1 – мастрихт–лютески гранитоиди; 2 – рудни жили Maastrichtian–middle Eocene Rila-Western Rho- dope batholith (quartz-diorite, granodiorite, granite, aplitoid-pegmatitic granite) is observed to the SW. Numerous deposits, mainly within the metamor- Chalcopyrite, tennantite-tetrahedrite, scheelite and phic rocks and rarely in granite, are developed in hematite are less common. Native gold, electrum, this area. The Golak skarn Fe ore occurrence (Kan- pyrrhotite, rutile, xenotime, argentite-acanthite, jal- ourkov, 1964, 1988; Vatsev, Tuparev, 1965f18), paite, cosalite, shadlunite, etc., are rarer. However, Golyamo Belovo polymetallic ore occurrence and the economic mineralization consists of native gold Akandzhievo-2 (Layno Dere) Sb ore occurrence and electrum, which defines the type of the ore. (Atanasov, 1974f19) were found. Numerous small- The Au-Ag phases predominate in association with er ore occurrences or mineralizations such as the pyrite and arsenopyrite. The gangue minerals are mainly quartz, lesser amounts of sericite and rarely chlorite, muscovite and calcite (Vidinli, 2015). The 17 Valkov, V., H. Borisov, M. Hristanova, Ts. Chontova, N. Valkova, T. Tonkova, N. Nenov, V. Velev, D. Spasov, V. Nenova. secondary minerals are developed to 150 m in depth 1972f. Report on the Geology of the Western Rhodopes Part between and are represented by iron hydroxides, jarosite, Dospat Village and Vasil Kolarov Dam, Geological Mapping at a Scale bornite, limonite, malachite, cerussite, etc. 1:25 000. National Geological Fund, report ІV-0247 (in Bulgarian). The Pisani Skali ore occurrence is situated NW 18 Vatsev, M., P. Tuparev. 1965f. Report on the Results of Accom- plished Geological Exploration and Prospecting of Skarn-Magnetite from the village of Medeni Polyani, 20 km SW Ores in Golak Village Area – Sofia District. National Geological Fund, from the town of Velingrad. Coarse grained Maas- report І-0600 (in Bulgarian). trichtian–Lutetian granite with occurrences of fine 19 Atanasov, G. 1974f. Report on the Results from the Geological Exploration Implemented in Ore Occurrences Hr. Danovo (Damla grained granite and pegmatite are exposed in the Dere), Plovdiv Area and Akandzhievo, Pazardzhik Area. National Geo- area. Series of multiple faults with NE direction (30– logical Fund, report І-0848 (in Bulgarian).

68 Akandzhievo and Dabravite Cu, the Bora, Vetren basement is composed by high grade metamorphic Dol and Chakarsko Dere polymetallic, the Chaira rocks (gneiss, gneissic schist, schist, amphibolite, Cu-Mo, and others are described as well. marble and metabasite, Kozhoukharov et al., 1992, The Golak Fe ore occurrence is located between 1993, 1994). Series of small granitoid intrusives the town of Kostenets and the village of Golak. The like the Yugovo, Dobralak and Topolovo plutons, earliest mining of Fe ore here has been established as well as numerous small stock-like or dyke-like between VI century BC and III century AC, and was bodies in the Mihalkovo village and the town of renewed in the XII and XV centuries (Konyarov, Batak areas, are intruded within the metamorphic 1940). High grade metamorphic rocks and Upper rocks. The data by different authors show that they Cretaceous granodiorite are exposed in the area. are Maastrichtian–Lutetian in age (Kožuharova, ESE faults are traced as the Vologarski fault is the Kožuharov, 1962; Yordanov et al., 1962; Nedial biggest one (Kanourkov, 1964; Vatsev, Tuparev, kov et al., 1998a; Dabovski et al., 2009; Marchev 1965f). Infiltrational skarns are formed in the meta- et al., 2013). The metamorphic and granitoid rocks morphic rocks and are represented by pyroxene and are overlaid by Tertiary terrigenous sediments and garnet, partly replaced by amphibole, epidote and volcanic rocks in some places. The Yugovo-Nare- quartz. The skarns are developed along the schis- chen and Mihalkovo ore fields as well as the Batak tozity in the biotite gneiss or in the marble lenses. mineralized area, are defined within this ore region. Magnetite ore is formed in the silicate rocks and he- The Yugovo-Narechen Ore Field is situated matite ore in the carbonate ones. The magnetite ore south from the town of Asenovgrad, and it reach- is represented by two types: (a) disseminated and es the town of Laki to the south. The high grade nest-like mineralization attached to the pyroxene metamorphic rocks (gneiss, gneissic schist, schist, in the skarns, and (b) compact irregular or strips of leptynite, amphibolite and marble) are exposed. The quartz-magnetite mineralization, formed during the granitoid rocks from Yugovo pluton are represented acidic stage. The hematite ore is represented by he- by series of small intrusive bodies like Dobralak matite and quartz together with unreplaced carbon- and Topolovo plutons (Kožuharova, Kožuarov, ate and skarn minerals. The quartz-hematite meta- 1962; Marchev et al., 2013) and are intruded in the somatism is accomplished during the acidic leach- metamorphic rocks. Paleogene sedimentary and ing on the carbonate rocks (Kanourkov, 1964, 1988; volcanic rocks are observed as well (Kozhoukharov Vatsev, Tuparev, 1965f). et al., 1994). Numerous Alpine fault structures are The Golyamo Belovo polymetallic ore oc- formed, such as the equatorial Bachkovo-Byala currence is found near the homonymous village. Cherkva fault sheaf, which is more than 25 km long Gneiss, biotitic schist and marble are outcropped and 4–5 km wide, the ENE Oryahovo-Bachkovo in the area. Small slant faults are observed in the Zone (Kozhoukharov et al., 1994), and series of marble. Quartz-calcite veins 2–30 m long and 5–10 sub-meridional faults are present as well. cm thick are found, and up to 20 cm thick nests are The ore field includes Mo-fluorite, W, Pb-Zn observed in some places. Galena, sphalerite, chal- and U ores, formed by hydrothermal processes, cocite, malachite, azurite, and limonite are dissemi- related to the Yugovo pluton. Yugovo (southern) nated in the veins (Kanurkov et al., 1960f20). and Narechen (northern) sectors are distinguished, The antimony Akandzhievo-2 ore occurrence is as they were separately described in the past. The located 7 km NE from the town of Belovo. Gneiss Mo-fluorite ores are observed in the southern sec- and marble, as well as Upper Cretaceous dacite, di- tor and the W ores are in the northern sector, while orite, granodiorite and andesite dykes are exposed. the U ores are spread over the entire territory, but Fault zone with 100–150° direction and 35–80° predominantly in the Narechen sector. Exogenous dip to SW is traced. 80 m long and 0.1–10 m thick U mineralizations are determined as well. quartz vein is determined. The ore is represented by The Mo-fluorite ores are developed in the Yugo- antimonite in quartz veins, nests and one ore lens vo (Fig. 11) and Tarnena Barchina deposits and in with length of 50 m and thickness up to 1 m (Atan- the Laki, Kumin Dol, Osikata, Propul and other ore asov, 1974f). occurrences. They are formed mainly in ESE to SE The Rakitovo-Bachkovo Ore Region covers and more rarely in NNE or ENE faults. The faults the northern parts of the Western Rhodopes, be- intersect the high grade metamorphic rocks, which tween the towns of Rakitovo and Laki (Fig. 2). The are sericitized, kaolinized and silicified. The ore bodies are represented mainly by ore veins. Meta- somatic bodies in the marbles are found as well. 20 Kanurkov, G., A. Kiselov, B. Velinov, L. Perev. 1960f. Report They are composed by quartz, fluorite and barite in on the Results from Revision Geological Exploration and Prospecting various proportions, more rarely by celestine and of Polymetallic, Molybdenum, Iron and Manganese Ores, Carried Out manganocalcite. Molybdenite, quartz-fluorite, fluo- During 1956 and 1957. National Geological Fund, report І-0499 (in Bulgarian). rite-barite and fluorite-carbonate ore types are dif-

69 and more rarely pyrite, bismuthinite, molybdenite and the gangue minerals are quartz and some calcite. The ore occurrence associates with quartz- monzodiorite (adamellite) body, which shows the relation with the Yugovo pluton (Naumov, 1951f22; Yovchev, 1978f23). The U ores are of two types: hydrothermal and exogenous (infiltrational). The hydrothermal ores are developed in the Narechen, Daikova Zona, Yu- govski Uchastak deposits, Yugovo-2 ore occurrence and others. They are hosted in equatorial faults as the rocks are silicified, sericitized, chloritized, hem- atitized and microclinized. The ore bodies are vein- like, lenticular and nest-like in shape, located in the tectonically brecciated contacts between granodi- orites and metamorphic rocks. The ore mineralization is represented by pitchblende (nasturane) and residues of uranium minereals. Magnetite, hematite, pyrite, molybdenite, marcasite, sphalerite, galena, chalcopyrite, bornite, bismuthinite and rammels- Fig. 11. Geological map of the Yugovo molybdenum-fluo- bergite ore and quartz, calcite and adularia gangue rite deposit (after Angelov, Angelova, 1972f) minerals are also found (Bedrinov et al., 1994f24; 1, granite; 2, marble; 3, gneiss and schist; 4, ore vein Bozhkov, Zabadanov, 1994f25). Фиг. 11. Геоложка карта на молибден-флуоритовото The exogenous ores are developed in Narechen находище Югово (по Angelov, Angelova, 1972f) and Byala Cherkva deposits and numerous ore oc- 1 – гранити; 2 – мрамори; 3 – гнайси и шисти; 4 – рудни currences (Bachkovo, Likovets, Razdelna, Do- жили bralak, Zdravets-2 and others). Their position is determined by the Bachkovo-Byala Cherkva faults, which are ore-conductive and partly ore-hosting. ferentiated. The main ore mineral is molybdenite, Slant interbedding faults or cracked zones are traced the main gangue mineral is fluorite and minor is around them. The ore bodies are bed and vein-like barite. Pyrite, sphalerite and in lesser extent of ga- in shape. The bed-like ores are formed along the in- lena, chalcopyrite, marcasite, magnetite, hematite, terbedding faults, concordant with the beds or along uraninite and others are also observed. Iron hy- the schistosity, as the vein-like ores are formed in droxides, covellite, chalcocite, renardite, cerussite, the steep faults. The ore mineralization is represent- anglesite, malachite, azurite, molybdenum ochres, ed by torbernite, autunite, rarely meta-torbernite and gypsum and sulphur are found as secondary miner- 21 meta-autunite. Limonite formed after pyrite is also als (Angelov, Angelova, 1972f ). documented. Probably the U is mobilized during the The small Pb-Zn ore occurrences Braykovitsa exogenous oxidation of the U enriched leptynite or and Komin Dere are found in the northern sector. primary ore minerals (Bozhkov, Zabadanov, 1994f; The main minerals are galena, sphalerite and quartz, Bedrinov et al., 1994f). minor are pyrite, molybdenite, chalcopyrite, fluo- The Mihalkovo Ore Field is located in the Western rite, calcite, ankerite and barite, and rare minerals Rhodopes, in the Mihalkovo village area. High grade are tetrahedrite, tennantite, aikinite, magnetite, he- metamorphic rocks (gneiss, gneissic schist, schist, matite, and bastnaesite (Kolkovski, 1989). amphibolite and marble) are exposed, in which small The W ores are developed in Narechenski Bani ore occurrence. Smaller ore occurrences and mineralizations of W, Bi and Mo (Yugovi Hancheta, 22 Naumov, A. 1951f. Final Report on the Accomplished Geo Lyuti Dol, Sveti Georgi-2, Levi Tsarvul and oth- logical and Mining Exploration in Narechen Ore Place – Asenovgrad ers) are also found. The Narechenski Bani ore oc- Area. National Geological Fund, report І-0231 (in Bulgarian). 23 Yovchev, Y. 1978f. Report on the Narechen Tungsten Deposit currence consists of 9 ore-bearing quartz veins in in the Northern Parts of Central Rhodopes. National Geological Fund, one NE fault zone. The host rocks are sericitized. report І-419 (in Bulgarian). The ore mineralization is represented by scheelite 24 Bedrinov, I., L. Dragomanov, G. Skenderov. 1994f. Explanatory Notes to the Legend of the Metallogenic Map of Uranium of the Repub- lic of Bulgaria. Scale 1:200 000. Smilyan Map Sheet. National Geologi- 21 Angelov, A., M. Angelova. 1972f. Report on the Geological cal Fund, report І-1225, 135 p (in Bulgarian). Exploration Implemented in Yugovo Fluorite-Molybdenum Deposit, 25 Bozhkov, I., D. Zabadanov. 1994f. Report on the State of the Laki Ore Field, Smolyan District. National Geological Fund, report ІІ- Uranium Reserves in Narechen deposit. National Geological Fund, re- 0720 (in Bulgarian). port І-1208 (in Bulgarian).

70 Fig. 12. Geological cross-section across the Gagovi Nivi fluorite deposit (after Todorov, 1974) 1, marble; 2, gneiss and schist; 3, amphibolite; 4, migmatite gneiss; 5, fluorite mineralization; 6, fault Фиг. 12. Геоложки разрез през флуоритовото находище Гагови ниви (по Todorov, 1974) 1 – мрамори; 2 – гнайси и шисти; 3 – амфиболити; 4 – мигматитови гнайси; 5 – флуоритова минерализация; 6 – разлом

intrusives and veins, most likely Maastrichtian–Lu- The fluorite ores are developed in the Neychov tetian, are intruded (Kozhukharov et al., 1963f; Sol- Chiflik, Gagovi Nivi, Petvar, Kirezlika, Mineralen datos, et al., 2008; Dabovski et al., 2009). Faults Izvor, Baalaka deposits and numerous ore occur- with NNW (320–350°) direction, as Bukovitski, Pet- rences such as Koteshnitsa, Shtrebel, etc. Their po- var, Chiflika, etc., sub-meridional (0–10°) and ENE sition is controlled by NNW Bukovitski, Petvar and (65–85°) are traced (Todorov, 1973). The Mihalkovo Chiflika faults (Todorov, 1973). The fluorite ore Ore Field is characterized mainly by series of fluorite bodies are bed-like in shape (Fig. 12) and are lo deposits with economic value. They associate with calized in marble beds in the high grade metamorphic skarn Fe and insignificant hydrothermal Mo, Cu, Zn complex. The ores are formed in the upper levels and Pb ore occurrences and mineral indications. of the marble, just below biotite, amphibole-biotite The Fe ore occurrences are found mainly be- schist, amphibolite and biotite gneiss. Interbedding tween the villages of Mihalkovo and Lyaskovo. ruptures and delaminations are formed along the Traces from ancient Fe production industry were contacts between the carbonate and aluminosilicate found (Konyarov, 1940). Infiltrational skarns are rocks. Hydrothermal-metasomatic quartz-jasperoid observed between marble and gneiss or in gneiss zones with maximum thickness of 15–20 m are de- only and they are represented by diopside, garnet, veloped. Nest-like, lenticular or irregular in shape actinolite, and epidote. The Mihalkovo, Lyasko- fluorite bodies are differentiated within the metaso- vo-2, Kabite, Stankovitsa, Nivishteto and other matic zones (Todorov, 1973). The hypogenous min- ore occurrences are found. The ore is formed erals are represented by fluorite, quartz, chalcedony, along interbedding fractures, rarely in steep NE calcite, montmorillonite and others. The kaolinite, or NW faults. The ore mineralization is represent- meta-halloysite and hydromica are minor miner- ed mainly by magnetite, more rarely by hematite. als, while the barite, dolomite, opal, lithioforite, Pyrite, chalcopyrite, galena as well as quartz, goethite (?), galena, sphalerite, pyrite, chalcopyrite calcite, barite and fluorite are also present (Kon- and molybdenite are rare. Hydrogoethite and more yarov, 1940; Kostov, 1947f26, 1948f27; Kackov, rarely malachite and azurite are found as superge- 1962f28; Kanurkov, 1988). nous minerals. Traces of quartz-sulfide and quartz- chalcedony mineralizations with fluorite pockets are observed within faults.This fact marks their ore 26 Kostov, I., 1947f. Preliminary Report on Geological Mountain conductive role (Todorov, 1973, 1974, 1989). Exploration of the Sites: Iron-Copper Ore Deposits between the Vil- lages of Patalenitsa (Pazardzhik Area), Byaga (Peshtera Area), Mi- The Batak mineralized area covers part of the halkovo (Devin Area), and Shipka Balkan, Kazanlak Area. National Northern Rhodopes, in the region of the towns of Geological Fund, report І-0043 (in Bulgarian). Batak and Rakitovo, the villages of Dorkovo, Kosta- 27 Kostov, I. 1948f. Report on the Iron Ore Deposits around the Village of Lyaskovo, Devin Area. National Geological Fund, report dinovo and Nova Mahala and Tsigov Chark resort І-0045 (in Bulgarian). 28 Kackov, N. 1962f. Preliminary Report on the Results from the Geological Mapping and Prospecting of Mineral Resources in Scale the Village of Krichim. National Geological Fund, report IV-0116 (in 1:25000 along the Vucha River Valley between the Town of Devin and Bulgarian).

71 (Fig. 2). High grade metamorphic rocks and numer- interbedding in the marble (Stara Reka) or amphi- ous Maastrichtian–Lutetian stock-like or dyke-like bolite (Semiza and Kachak Chark) with scheelite, magmatic bodies are outcropped. They are overlaid bismuthinite and pyrite. Skarn mineralizations are in some places by younger post-ore Tertiary vol- discovered in the marble (Savov, 1970f30). canogenic and terrigenous rocks. The polymetal- The Barutin-Smilyan Ore Region is located in lic Removo ore occurrence and Vlasachina, Dul- the SW part of the Rhodopes Mountains, southern duran, St. Ilia, Manastira, Chetvarti Prozorec and from the towns of Dospat and Smolyan, and parts other mineral indications are found in the area. The of it spread in the territory of Greece (Fig. 2). The Pb-Zn Beglika ore occurrence and Sharovi Livadi, basement is composed by high grade metamorphic Mahalite and Starata Reka mineral indications are rocks as gneiss, gneissic schist, migmatized gneiss, also discovered. Moreover, the W-Bi Suhata Reka, amphibolite, marble, etc. The Maastrichtian–Lute- Kachakov Chark and Semiza ore occurrences, as tian Dolno Dryanovo, Barutin-Buynovo (Elatia) and well as the mineral indications of Cu (Bregovo, Smilyan plutons are intruded in the basement. The Tsigov Chark), Mo (Hremshtitsa, Lepenitsa) and Fe metamorphic rocks and plutons are transgressively (Kostandovo, Mazar Dere-South, Nova Mahala), overlaid by Tertiary sedimentary and volcanic rocks are also noted. (Kozhoukharov et al., 1993). Skarn Fe and hydro- The Removo ore occurrence is situated 13–14 km thermal W, Mo, polymetallic, Au-polymetallic ores west from the town of Batak and 8 km SE from the are formed in this ore region in relation to the evolu- town of Velingrad. Marble, amphibolite, chlorite tion of the mentioned plutons. All of the discovered schist, gneiss, diorite porphyrite dykes and Paleo- ore mineralizations do not have an economic value gene sediments are observed. Ancient works (pits, and are defined as ore occurrences or mineral indi- trenches) and metallurgical slags are discovered. cations. The Dolno Dryanovo, Barutin and Smilyan Fault zone with 320–330° direction and 25–40°, ore mineralized areas are outlined in the ore region. rarely up to 60° dip is formed along the marble beds The Dolno Dryanovo mineralized area covers (Tretyakov, Ivanov, 1953f; Kozhukharov et al., part from the SW slopes of the Rhodopes Moun- 1958f). The zone is traced up to 1000 m in length tains, at about 12 to 25 km from the town of Got- and its thickness is from 0.3 to 20 m. The marble se Delchev (Fig. 2), in the area of the villages of around the fault is quartzitized and limonitized. The Satovcha, Dolno Dryanovo, Krushevo, Valkosel, ore mineralization is represented by veinlets, dis- Fargovo, Kochan, etc. The position of the mineral- seminations and nests with galena, sphalerite, chal- ized area is defined by the development of Maas- copyrite, pyrite, rarely argentite and markasite. The trichtian–middle Eocene Dolno Dryanovo granite ore is low-grade, as higher concentrations of Pb, Zn pluton. It is compound by porphyroid and aplitoid and Co are found in separate samples only. granites intruded in high grade metamorphic rocks. The Beglika ore occurrence is located about The following ore occurrences are found in this 12 km SSW from the town of Batak. Leptynite, am- area: Krushevo skarn Fe ore occurrence; Satovcha, phibolite, marble, gneiss and schist are exposed in Fargovo, Ablanitsa hydrothermal polymetallic ore the area and to the East they are overlaid by Oli- occurrences and other smaller mineralized indica- gocene volcanic rocks. Three NW-trending faults tions (Valkosel, Bardeto); W mineralizations near (320–340°) with quartz veins are distinguished. The the Fargovo village and the Satovcha-2 and Dolen host rocks are sericitized, kaolinized, chloritized, U occurrences. quartzitized and pyritized. Iron and Mn hydroxides The Krushevo Fe occurrence is of skarn type. are determined in the veins, while primary ore min- It is located between the villages Krushevo and erals are not observed. Rock pieces with galena, Debren, about 14 km NE from the town of Gotse pyrite, magnetite, hematite, chalcopyrite, cerussite, Delchev. The ore occurrence’s area is composed by anglesite, Fe hydroxides, etc., are found. Increased high grade metamorphic rocks – biotite and mus- contents of Pb, Zn, Ag and lesser amounts of Cu covite gneiss, schist, marble and amphibolite. The and Au are determined in some samples (Shilyafov ore mineralization is discovered in one interbedding et al., 1972f29). fault, traced within bed of muscovite gneiss and The W-Bi small ore occurrences and mineraliza- marble. Infiltrational Ca-skarns are formed along tions Suha Reka, Semiza and Kachak Chark con- the interbedding fault and are composed by pyro sist of ore veinlets, nests and lenses, which form xene, garnet, magnetite, amphibole, epidote, quartz and hematite. Three sectors are differentiated within

29 Shilyafov, G., Zh. Dineva, M. Hristanova, Ts. Chontova, H. Bo- risov, A. Sukov, T. Tonkov, Y. Tsvrtanov, D. Spasov. 1972f. Report 30 Savov, K., 1970f. Report on the Results from the Implemented on the Geology of West Rhodopes Part between the Village of Dospat Detail Prospecting for Scheelite-Bismuth and Polymetallic Ores South and the Town of Devin. Geological Mapping in Scale 1:25 000. Na- eastern from the Town of Velingrad – Western Rhodopes. National tional Geological Fund, report ІV-0241 (in Bulgarian). Geological Fund, report І-0767 (in Bulgarian).

72 the ore occurrence: Dalbi Dol, Krushevski Dol and Borino, Buynovo, Marashova Chuka, Chavdaritsa, Tikla. The ore bodies are bed-like, localized within Zmeitsa-Chala and some smaller mineral indica- the interbedding fault, and in Tikla sector – in the tions (Barutin, Vaklinovo, Kozhari, Lyuti Dol, marble. The main ore mineral is compact magnetite. Tsrancha, etc.), are formed during the late evolution Hematite is rarely observed, together with quartz. phase of the pluton. Pyrite, chalcopyrite, pyrrhotite, etc., are determined The Mo Zmeitsa–Mursalska Reka ore occur- in small veins, and ~5000 tons of ore have been ex- rence is 2 km SE from the village of Zmeitsa, where tracted (Boyadjiev, 1953f31; Kanurkov, 1988). the granite from the Barutin-Buynovo pluton is ex- The polymetallic Satovcha, Fargovo-2, Ablan- posed . Ore controlling fault trending at about 45° itsa ore occurrences and Valkosel and Bardeto and a system of large fractures with direction of mineral indications are connected to the faults 320–340° is observed. Around these structures the intersecting the metamorphic and granite rocks. rocks are affected by advanced argillization, kao- Most often, the faults have strike of 300 to 330°, linization and limonitization. The ore is represented and in Fargovo-2 ore occurrence – from 60 to 110°. by molybdenite, which forms small ore nests. Pyrite Around them, the rocks are altered by sericitiza- and relicts of chalcopyrite are observed as well. In- tion, muscovitization, chloritization, kaolinization significant contents of Pb and Zn are also discov- and advanced argillization. Iron and lesser amount ered (Shilyafov et al., 1972f). of Mn hydroxides are developed. The presence of The polymetallic Zmeitsa-Chala, Buynovo, Ko low-grade Pb, Zn and Cu mineralization is deter- zhari, etc. ore occurrences are also located in the mined only by spectrometric studies (Slavov et al., granite of Barutin-Buynovo pluton, rarely near the 1972fa32, 1972fb33). contacts with marble. Mostly NW (320–345°) and The U Satovcha-2 and Dolen ore occurrences rarely NE to equatorial faults (50–90°) are deter- are located near the homonymous villages. The first mined. The rocks are advanced argillized, kaolin- one is formed in brecciated zone along the contact ized and limonitized. At the surface the ore min- between Dolno Dryanovo granite and metamorphic eralization consists of pyrite and Fe hydroxides. rocks, and the second one – between muscovite and Chalcopyrite, As-Ag sulfosalts and löllingite are biotite gneiss. The brecciated rocks are argillized observed in polished sections. The presence of Pb and mineralization of autunite and uranium soot is and Zn is also noted (Shilyafov et al., 1972f). found in them (Skenderov et al., 1994f). The Smilyan mineralized area is located 10– The Barutin mineralized area is located south 15 km south from the town of Smolyan, in the vi- from the towns of Dospat and Devin, in the area of cinity of the villages of Smilyan, Arda, Mogilitsa, the villages of Barutin, Zmeitsa, Tsrancha, Chavdar, Borikovo, etc. High grade metamorphic rocks are etc., and to the south it extends in Greece (Fig. 2). exposed in this area and are represented by different It is controlled by the Maastrichtian–middle Eocene gneisses, gneiss schists, marbles and amphibolies. Barutin-Buynovo pluton, intruded into high grade The Smilyan pluton is intruded into metamorphic metamorphic basement. The pluton is composed rocks and is composed by medium to fine grained mainly by medium grained granite, while grano- granite, fine grained pegmatoid and aplitoid granite diorite and fine grained granite with pegmatite and and vein bodies with mineral composition reach- aplite veins are developed in its endocontact parts ing that of granosienite and granodiorite (Stefanov (Kozhoukharov et al., 1993). Oligocene volcano- et al., 1957f34), which are included in the group genic and terrigenous rocks and Neogene–Quater- of Maastrichtian–middle Eocene plutons (Kaiser- nary sediments overlay the marginal part of the plu- Rohrmeir et al., 2013). Paleogene sedimentary and ton. Series of ore occurrences, such as the molyb- volcanogenic rocks overlay the granite and meta- denum Zmeitsa-Mursalska Reka, the polymetallic morphic rocks. Albitization, greisenization, argillic and advanced argillic alterations are developed in separate parts 31 Boyadjiev, S. 1953f. Report on the Geological Exploration of of the Smilyan granite. Several ore occurrences are the Debren-Krushevo Iron Ore Deposit, Gotse Delchev Area. National found and are conditionally determined as Au-Ag- Geological Fund, report І-0305 (in Bulgarian). polymetallic (Chereshkite, Rotat, Posyak, Smilyan, 32 Slavov, I., T. Todev, M, Todeva, Ya. Milanova, V. Sirkatova, V. Valkov, T. Todorov, Y. Vodenicharov. 1972fa. Report on the Geology etc.). The ore mineralization is variable, with low of Part of the Western Rhodopes, Stargach Mountain and Gotse concentrations of the elements. Pyrite, galena, Delchev Valley. Geological Mapping and Prospecting of Mineral Resources at a Scale 1:25 000. National Geological Fund, report ІV- 0244 (in Bulgarian). 33 Slavov, I., Ya. Milanova, Y. Vodenicharov, A. Sukov, S. Stoev, 34 Stefanov, N., E. Maslenkova, K. Katsarska, D. Stefanova, G. Baltakov. 1972fb. Report on the Geology of Parts from the Western K. Netsov, V. Mihova, P. Todorov. 1957f. Report on the Complex Rhodopes and Dospat Valley. Geological Mapping and Prospecting of Geological Mapping at 1:25 000 Scale, Carried Out in the Eastern Mineral Resources at a Scale 1:25 000. National Geological Fund, re- Part of Western Rhodopes, between the Towns of Smolyan and Madan. port ІV-0245 (in Bulgarian). National Geological Fund, report ІV-0064 (in Bulgarian).

73 sphalerite, chalcopyrite, molybdenite, native silver, analysis shows certain substaintial magmatic spe- gold as well as barite are observed but their presence cializsation of this complex, characterized mainly differs in the separate ore occurrences. The Kashlite by thungsten, molybdenum, fluorite, uranium, ore occurrence with increased contents of rare earth lesser iron, bismuth, antimony and insignificantly metals is also noted (Kolkovski, 1989; Tsvetanov et lead, zinc and copper. The geological and minings al., 1993f35; Dushkov, Bozhurska, 1993f36). exploration works discover uranium, thungsten, molybdenum, molybdenum-thungsten, molybdenum-fluorite, gold-molybdenum, thungsten-molyb Conclusion denum, bismuth, iron, fluorite, antimony, gold- bearing antimony, polymetallic, gold-polymetallic The Rila-Rhodope Upper Maastrichtian–Lutetian and copper types of ores. The uranium (Beli Iskar, granitoid complex, associated with Eocene Illyrian Beslet, Narechen), fluorite (Mihalkovo) thungsten fold and thrust-nappe deformations, is differenti- (Grancharitsa), gold-molybdenum (Babyak), anti- ated during the collisional stage from the evolution mony (Ribnovo), iron (Mihalkovo, Lyaskovo) and of the Balkan Orogenic System. The metallogenic some other deposits possess probable economic importance. The regional analysis determines the 35 Tsvetanov, D., I. Kalinova, M. Kolarov. 1993f. Report on the positions of the different ores related with the Geological Maping and Prospecting of Mineral Resources in the noted plutons, the composition of the host rocks, Central Rhodopes Ore Region (Smilyan, Arda Villages and other) the metasomatic alterations and the peculiarities at a Scale 1:25 000. National Geological Fund, report ІV-0397 (in Bulgarian). and orientations of the ore hosting fault structures. 36 Dushkov, A., S. Bozhurska. 1993f. Report on the Results from Based on these data, the Rila-Western Rhodopes, the Implementation of the Geological Task: Summary of the Geological Rakitovo-Bachkovo and Barutin-Smilyan ore re- Exploration Works Accomplished in the Area of Chereshkite Ore Occurrence and Smilyan Granite Intrusive. National Geological Fund, gions with individual ore fields or mineralized ar- report І-1097 (in Bulgarian). eas are defined.

References

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