I. INTRODUCTION

Geographically, Romania is located in Central Europe, at nearly the same distances far from Ireland, North Cap and Sverdlovsk (Fig. 1).

~ __ ___ .. _____ L ___ ___ _ -=--.....----=~'__.l...._L _ ___ ... J

Fig. 1 - Romania: Location

In European terms, Romania is rich in mineral potential, especially oii, gas, salt, gold and silver ores and non-ferrous metals. Historically, the Romanian mining industry has frequent1y been at the forefront of European development, often leading the way to the identification and evaluation of deposit types tha! have subsequently proved to be of major importance elsewhere.

In Romania varied ore deposits have been exploited from the earliest times, gold, copper, lead, zinc, manganese, iron and salt having been worked extensively.

Archaeological evidence suggests that there has been mining in Romania for thousands of years, with artifacts from various ages having been shownto have beep made from locally produced metals and minerals. Ore production became better organised during the Roman period, while simultaneously processing techniques became more diversified (Borcoş et al., 1994).

8

The earliest mineral working for which evidence exists was Palaeolithic flint and stone production, the sites ofseveral "workshops" having been identified (Fig. 2). Gold production commenced at Cireşata in the Brad district of the Apuseni Mourttains during the Neolithic period (10,000-1,900 BC) both from hard-rock and alluvial deposits; salt was also produced at this time from the Moldova region, and possibly copper. Artifacts indicate that copper smelting and casting were practici sed, and coloured ceramics from this period show

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Fig. 2 - Mining activity in the Palaeolithic-Neolithic period (ace. to Borcoş et al., 1994). Key: Palaeolithic: 1 - areas of abundant archaeological discoveries; 2 - unconnected archaeological sites; 3 -extraction sites. Neolithic: 4 - areas of abundant archaeological discoveries; 5 - unconnected archaeological

sites; 6 - extraction sites; 7 - stone, flint; 8 - salt; 9 - gold.

that manganese was used as a pigment. . During the Bronze and early Iron Ages, gold and copper were produced in

. Transylvania, and in the Banat, Oltenia and Dobrogea districts (Fig. 3). Gold production was also centred on the Metaliferi Mountains, in the Brad district and probably at Roşia Montană.

Salt was produced through evaporatioD., and bronze, gold and iron production was widespread.

Between 450 BC and 106 AD in the Geto-Dacic period, underground rnÎning commenced for gold, other metals and for salt (Fig. 4). Large-scale quarries were opened for building stone, and metallurgical technology progressed, with the introduction of reducirig furnaces for iron ore. Bronze, gold and silver metallurgy and manufacture also developed, the :scale of gold production being indicated by the 165,000 kg of gold that were taken to Roma as spoils ofwar by the emperor Trajan.

Fig. 3 - Mining activity in the Bronze and First Iron

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J •

''V s. ,~

7 X 8_ 9 c:::J 10_

el al., 1994). 1 - areas of abundant Palaeolithic and Neolithic archae:oloigical l'I,:c,..n,,,"r, 2 - unconnected archaeolo-

sites in the bronze age; 3 unconnected archaeological sites in the tirst Iron Age; 4 extraction sHes; 5 bronze processing centres; 6 areas of abundant Bronze and First Iron archaeological discoveries; 7 -

irOD processing centres; 8 - salt; 9 - gold; 10 copper.

9

Mining activity increased during the Roman period with intensive working of deeper deposits as weB. production Încreased from iron and copper smelting, silver output was derived fr9m non-ferrous ores and cinnabar was produced for use as a dye. Existing centres gold, silver and salt production included the Metaliferi and Poiana Ruscă Mountains and the Banat district, and new centres appeared in the Rodna and Baia Mare district.

Metal and mining continued after the Roman period, new deposits identified worked and cast iron being produced for the time (Fig. 5). Between the 1 and 17th new mining technologies were introduced, water-powered stamps carne into use ore crushing. New deposits of copper, lead, zinc, iron and manganese were also found in the East during time, .and towards the end of the period the first records of the country's heritage were produced. The second half of 17th Century marked the appearance of the first institutions main goals were to organise, supervise (local offices, masters' comrnissariats and inspectorates) and settle (mining tribunals and courts of law) actlvlty. first mining carne force 1854,

replaced 1924 by a new on the constitution of the unitary Romanian

10

Î 'O 2<=)

J lfD °Orad .... 4 c::J S_

I IIIIIIII 7 mIIII Il

Fig. 4- - Mining in the Second Iron and Roman periods to Borcoş et al., 199-') 1 active sites in the Roman 2 active mining sites in the Geto-Dacic

period~ 3 salt~ 4 - 5 - copper; 6 iron; 7 - 8 - building stone.

• The industrialisation of the industry since the mid-19lh Century included the introduction of modern explosives, mechanised drilling, and the use electrical power underground. Between 1890 and 1896 California stamps, roll mills ban were introduced ore reduction, copper calcining commenced in 1876 and in 1 7 Romania's tirst cyanidation gold plan opened.

The 150 have seen the compilation a amount data about Romania's mineral deposits and potential. AlI major ares of interest have been covered, including those of potential hydrocarbon interest. must also made to large number minerals were identified in RomanÎan deposits, including the element teUurium, which was discovered gold ore at the Faţa Băii ore deposit (Zlatna district) in the Metaliferi Mountains.

the numerous deposÎts been evaluated and have either exhausted or of criteria that do not apply in today's economic environment. As yet,

Httle opportunity to re-evaluate such occurrences, although the country's for and development a huge amount information <?n

aU aspects of deposit geolog);' and resource estimations, obtained from past dtilling programmes and thorough geological investigation. Even in recent exploration by the state hampered by lack of resources, and Îs thus potential for

Il

5 - Mining in the pre-feudal and feudal periods (ace.to Borcoş el al., 1994) Key: 1 active areas in the and Roman periods; 2 - active mining areas in tlle pre-feudal period; 3 active mining areas in ilie feudal period; 4 salt; 5 - gold; 6 - copper; 7 - 8 lead and zinc;

9 - mercury.

overseas investment in both grassroots exploration and re-appraisal properties about which substantial amounts of data already exist.

Recent geological and geophysical work shown that there are, in fact, many mineral prospects both near-surface and at depth that have considerable potential for further investigation, and that offer opportunities overseas investors interested in the country's mineral resources.

The most productive mining centres with . classical metalliferous ore deposits (containing gold, silver, eopper, iron and are loeated Neogene volcanic zones in the Metaliferi and Oaş-Gutâi Mountains (referred.to as types al and a2 respectively in Table 1), and in the",Banat region (b 1) and in the Bihor massif (b2) related to Upper Cretaeeous-Paleocene intrusive struetures, as well as in the East (el) and South Carpatmans in the Poiana Ruseă (e2), or in Dobrogea (c3), the Iatter related to

. Palaeozoic or older metamorpmc roeks. The significance of these worked intensively since aneient times, is shown by the amount of metals (extraeted and existing· potential) estimated for some of the representative ore deposits. .

12

MOBILE ZONES

From -both structural and metallogenetic points of view the Romanian territory belongs to the Alpine and represents a part the subgIobal Mediterranean (Tethyan)-Himalayan belt. .

Geomorphological units of Central and South-Eastern Alpine orogen are as follows: Eastern Alps, West East Apuseni Mountains, Transylvanian Basin, South Carpathians, Balkans-Srednagora, Pannonian Basin, Serbo-Maeedonian Massi{, Rodopi Massif, Dinarides, Albano-Hellenides (Fig. 6).

Romania eomprises the Carpathian Mountains chain, namely the. South Carpathians, Apuseni Mountains, with i~tramontaneous Transylvanian and Pannonian Basins, surrounded by the foreland (mainly plains in Moldova and Muntenia, eroded mountains in Dobrogea). major units are by two mobile Alpine regions, Carpathian and Northern Dobrogea, and pre-Alpine cratons (Moesian, Seythian and Moldavian platforms).

Carpathian chain is a (pre-Alpine and Alpine) bound westwards by the Alps and south-eastwards by the Balkans. It has a peri-cratonic position, south of the Eurasian Plate. This structure is built up in Romania inner units (North Apuseni moulded by external Carpathian arc (the Carpathians), as weB as South Carpathians whieh eonsist of basement and cover nappes, magmatic belts and massifs, sţdimentary post-tectonic structures.

basement nappes are built up pre-Mesozoic schists and Upper Paleozoic-Mesozoic sedimentary rocks (Inner Dacides, Median Dacides and Marginal Dacides). The Inner Daeides oceur in the North Apuseni Mts., as a prolongation of Austroalpine structure of the Alps; the tectogenetic event is pre-Gossau. The Median Dacides develop from the East to the South Carpathians. The innermost part of the

Carpathians ("Crystalline-Mesozoic zone") ·contains Bucovinian, Subbucovinian and Infrabucovinian nappes formed Hereynian and Austrian deformations. Bueovinian Unit proceeds to the West Carpathians, whereas the Subbucovinian and Infrabueovinian nappes eorrelate with Supragetie and Getic Nappes of South Carpathians, which were involved in Laramian deformations too. Supragetic mid Getic proceed to Serbo­Macedonian massif and farther to the Inner Balkanides, Rhodopi and Strandja; the Marginal Dacides oceur in the South Carpathians and were considered as Autochthon ("Danubian Modern interpretations divide into the Lower Danubian Unit and Upper Danubian Unit, both involved in pre-Alpine and Alpine/ Austrian and Lararman thrustings. Recent driUing data provide evidence of Danubian tbrusting over the Moesian

. Platform during intra .. Sarmatian defomiatlons. nappes built up ofMesozoic flyseh sediments and ophiolites are represented by

Transylvanides in the South Apuseni and East Carpathians and External Dacides in and South Carpathians (black flysch nappes proceeding to Ukraine

nappe to Eastern Serbia and Srednagora). The main teetogenetie events are Austrian and Lararman.

[l]]] 1

~2 ~3 ~4 ~5 ~6 [:=J7 E-;-j 8

ur:a 9

~10

Fig. 6 - Carpatho-Balkan orogen and adjacent areas (geotectonic setting according to Săndulescu, 1984; geomorphological parts according to various authors).

13

Key: EA - Eastern Alps; WC - West Carpathians; PB - P.annonian Basin; AM - Apuseni Mountains; TB -Transylvanian Basin; EC ~ East Carpathians; SC - South Carpathians; D - Dinarides; SMM -:- Serbo­Macedonian Massif; BS - Balkan-Srednogora; AH - Albanides-Hellenides; R - Rodopi. 1, Neotethysian suture; 2, adjacent sutures: a) Ceah1au. Severin-Strandja zone; b) Pindus-Serbian zone; 3, Ew:opean basement units; 4, pre-Apulian basement units; 5, Apulian/Pelagonian basement units; 6, cover units: a) Moldavides; b) outer Dinarides and Hellenides; 7, Post-tectonic cover; 8, North-Dobrogea; 9, platfonns: a) MQldavian (East European) platfonn; b) Moesian and Scythian platfonns; 10, Alpine magmatic rocks: a) Banatltes; b) Neogene igneous rocks.

14

Cover nappes built up ofUpper Cretaceous-Paleogene fiysch sediments and Miocene molasse in the East Carpathi~s that consist of (a relay of the Transylvanides, proceedings to Ukraine; the main tectogenetic events are Laramian and. Lower Miocene) and Moldavides (a group of nappes proceeding to Ukraine; the tectogenesis was multistage during tne Neogene

Magmatic and massifs of various are incprporated. in, or npYIP1"Y'l'Ifp parts of ahove-mentioned of nappes. Worth mentioning are' Danubian pre-Alpine

granitoides and, especially, two major petrogenetic of calc-alkaline the Laramian magmatic ("Banatites") in the Mts. - South Tertiary volcanic arc Carpathians with

Sedimentary post-tectonic structures South Carpathians, molasse depressions, that is yalm(Jlrualn post-tectonic covers throughout the whole Carpathian range.

and

The North Dobrogea area has no connection with the Carpathians and is a shorter-lived structure to them. This is the western part of a proceeding from the South and Greater Caucasus. It contains tectonic units built up of pre-Mesozoic anchimetamorphic and granitoids west, and prevailing and bimodal main compression during the Kimmerian tectogenesis.

PRE-ALPINE PLA TFORMS

Platform represents the Carpathian foreland the southern part of the country. It is into two sectors by the Intramoesian fault (Dobrogea sector and WaUacruan-Prebalkan sector). The basement is Precambrian' and the cover ranges from the Paleozoic to

The Scythian Platform with the Central Platform and corresponds to "Meso-Europa" (Stille, 1 ofEpihercynian ~ .. u,'UE>'

Moldavian Platform to the termination East European Platform, south of the Ukrainian Shield. The basement is Precambrian and the cover Precambrian to post-Precambrian.

GEODYNAMIC EVOLUTION OF THE ROMANIAN TERRITORY

geodynamic evolution Romanian territory followed successive cyeles of ocean and elosing Geologic, metallogenetic data' provide evidence for reconstitution more recent and settings. The only

of spreadinglcompression events belongs to cycle whereas pre-are represented by parts sequences incorporated in Alpine structur.es. present-day architecture of the Romanian territory is associated with the

development of the Tethyan trench (palaeo- and Neo-Tethys). Both short-lived anei more evolved rifts are characteristic of this setting and yielded various types of magmatic and

tauog,em~tlc products. Interpretation of ocean fioor subduction, collision and

15

post-collision events is sometimes difficult because of contradictory assessments about the use of plate/microplate/sialic block, subduction or subfluence, ophiolite meamng/significance (island arc andlor ocean floor spreading products), calc-alkaline volcanicity (subduction­related or rift-related magmatism), position to and correlation with the major Tethyan accept or refusal ofback-arc in the Carpathians etc.

Pre-Alpine geodynamic models-paleotectonic reconstructions in the Carpathians are difficult to ascertain. The Alpine evolution, according to recent interpretations (especially Săndulescu, 1983, IGCP Project nO.l etc.), is related to the main Tethyan suture, that is the Vardar zone and its prolongation crossing the Carpathian orogen. During the spreading period the Transylvanian oceanic area and the intracontinental rift of the Dacides occurred. Compressions gave rise to the actual curved Carpathian configuration and the complex nappe structures, whereas calc-alkaline magmatism is considered subduction type and assigned to the external Dacidic trough. An alternative hypothesis postulates the Înheritance of the Garpathian curvature (e.g. Vlad, 1980, 1986, IGCP Project no.169).

The distribution of the magmatic arcs suggests a restricted transversal arc migration; their pinning 1S aquiescent to compression of the above-mentioned narrow elongated troughs and arc behind the elaborate curvature of the East Carpathians. Different portions of the magmatic arcs exhibit changes in evolution, and petro­metallogenetic characteristics along strike and/or width; association with back-arc extensional products îs not uncommon.

The North Dobrogea geodynamic model is based on a complete orogenic evolution in Paleozoic (spreading compression with subduction and collision products), followed by rifting, formation of oceanic crust, deformation with thrusting during Kimmerian (Săndulescu, 1984). The alternative interpretation put forward the role pIayed by the intracontinental rifting with bimodal magmatism yielding an aulacogen-like faiJed arm linked with the Tethys through the Crimea and Greater Caucasus (Vlad, 1978). '

The metallogenic map of Romania (scale 1:2,500,000), prepared by Ianovici, Rădulescu, Dimitrescu, Krautner and Mirăuţă in 1966, was the first attempt to present the metallogenic elements of Romania in a systematic form. Subsequent1y the same method of presenting processes in terms of both time and space was used by Rădulescu, Borcoş, Krautner, Savu, Vasilescu in 1969 to produce a metallogenetic map of Romania on the scale of 1: 1,000,000. This shows the stratigraphical, geochemical and geodynamic control on the conditions of formation of the accumulations of metallic and non-metallic useful mineral resources, and also the posiţjon and particular characteristics of the 24 metallogenetic provinces defined.

According to the idea adopted, which is also used in the maps on a scale of 1:200,000 produced for the main mining regions of the country, a metallogenetic map,

of scale, represents the "genetic units" of mineral concentration with' typical areas of development. Each genetic unit Îs identified geographical and temporal terms as part the process of evolution by its particular conditions of accumulation,

16

typically reflected in the relationships between its genetic and geochemical characters and the processes of magmatism, sedimentation and metamorphism. It was decided that the basic unit may reasonably be consjdered to be the metallogenic province which, with rare exceptions, coincides with the corresponding petrological units. Detailed work carried out having regard to the geographical distribution of ore deposits, as also to their age and paragenetic and geochemical nature, led to the definin.g of subordinate metallogenic units - sub-provinces, zones, districts, fields - or even to the individual identification of a number of isolated deposits. This mode of presentation may be considered as classic and is able to provide the maximum amount of information needed for an understanding of the combination of circumstances which led to the formation of useful mineral resources. This information was subsequently used as a basis for the preparation of the scale 1: 1,000,000 maps of useful mineral resources in Romania- and of numerous prognostic maps and documents (Borcoş, Krăutner, Udubaşa, Săndulescu, Năstăseanu, Biţoianu, 1984).

The concept of plate tectonics conceming the Romanian territory was introduced in the geologicalliterature in the early 70's (e.g. Rădulescu, Săndulescu, 1973; Bleahu, 1974; Hertz, Savu, 1974 etc.).

First metallogenetic interpretation in terms of plate tectonics is due to Ianovici, Vlad, · . Borcoş and Boştinescu (1977) taking into account Romanian porphyry copper occurrences.

Subsequent significant contributions on plate tectonics and metallogenesis belong to Vlad, concerning North Dobrogea (1978) and Banat metallogenesis (1979), Cioflica and Vlad (1980, 1984), Vlad (1986) about Alpine metallogenesis, Folea, Vlad and Berbeleac (1987) referring to Cu-Pb-Zn metallogeny during Alpine and pre-Alpine Wilson cycles, Berbeleac (1988); Rădulescu, Borcoş and Săndulescu (1994) who correlated the main relations between geotectonics and metallogenesis during the Alpine time taking into account metallogenetic specialisation too, and Vlad, Borcoş (1994, 1997) on Alpine metallogenesis of the Romanian Carpathians.

* * *

Numerous ore deposits known and mined since Roman and even pre-Roman times (Au, Ag, Pb, Zn, Cu, Mn, Fe, etc.) have intensively been extracted, mainly the high-grade ores. Various metallic minerals were described as locus tipicus occurrences the world over from very well-known ore regions as Baia Mare, South Apuseni Mts and Banat. Baia Mare vein sets and the Gold Quadrangle are famous in the geological literature for their classical gold-silver deposits whereas skams from Banat are reference deposits ofthis kind.

The occurrenceldistribution of metalliferous deposits within the above-mentioned geotectonic framework · is various from both quantitative and qualitative view-points. Platforms contain restricted deposits (iron and copper ores) only in the Dobrogean realm. The mobile regions are characterized by minor Ba, Cu, Pb, Zn, Fe mineraIization in the North Dobrogea region and widespread mineralization throughout almost alI stratigrafical levels of the Carpathian orogen. The complex geological structure of the Carpathians explains the great variety of the genetic/paragenetic metalliferous types resulted during a Iong evolution, from Precambrian to Quatemary. In some cases, the remobilization played an important role in the diversification of primary ore forming processes. Metallogenetic heredity and metallogenetic

17

evolution in association with events of several Wilson orogen cycles are basic concepts that permit a correlation attempt between geological features controlling pulsative ore deposition du ring several cycles with the inherent geochemical behaviour of major metals, obvious especially for the Upper Paleozoic and the Alpine cycle. Consequently, Precambrian, Paleozoic and Alpine metallogenetic events are taken into account and reviewed below (Fig. 7, Plate 1).

PRECAMBRIAN METALLOGENESIS

Basement nappes of the Carpathians and a restricted area of Dobrogea expose in places were well preserved Fe, Pb-Zn and Cu-pyrite deposits assigned to undeveloped sequences of Wilson orogenic cycle/cycles. The Precambrian metallogeny represents on1y 5 % of the total resources estimates of the country. Iron ore predominates and builds 70% of the national iron potential. An overview on Precambrian metallogeny in the South Carpathians is given by Udubaşa (1987).

Metallogenesis associated with carbonate roda (possible equivalent to metallo­genesis related to intracontinental rifting, Vlad, Borcoş, 1997)

This activity is represented by Pb-Zn carbonate hosted occurrences found in the East and South Carpathians. The most signifieant deposits (e.g. Blazoa Valley) are found in the medium-grade metamorphosed Rebra Group ofUpper Proterozoic age (East Carpathians). lts

, middle part ("the carbonate formation") contains stratabound ores lenses (mainly pyrite, .- sphalerite, galena, chalcopyrite) related to silieate, graphite and quartz intercalations in

carbqnate roeks (Udubaşa, 1972/1996; Udubaşa et al., 1983). Minor occurrences of the same genetic type are located in the polymetamoprhic Făgăraş Group (South Carpathians).

Massive sulphide deposits (possible equivalent to metallogenesis related to ocean­floor spreading, Vlad, Borcoş, 1997)

The metallogeny is provided by mineralization of Cyprus-like type. Massive Cu-pyrite ores ·are found in the Precambrian polymetamorphic Altân Tepe (AT) series ofthe Dobrogean eraton (Fig. 8). The upper part of the Altân Tepe series (AT 2) exhibits a conspicuous volcano-sedimentary character and encloses sever_al "en eehelon" subverticallenses of massive sulphides (pyrite, chalcopyrite, magnetite, sphalerite, galena, pyrrhotite) surrounded by impregnation pyrite halo (Mureşan, 1972; Berbeleac, 1986). .

Restricted occurrences of this kind are found in the metabasitic middle part of the Bibaria series of Upper Proterozoic age (Bihor massif of the North Apuseni Mts). Theyare found in the Brusturi-Luncsoara-Poiana district and a reeognizable mobilization of metals during the Laramian metallogenesis is to be mentioned (Lazăr et al., 1980).

The Getic Nappe of the South Carpathians . contruns minor metagabbro bodies with disseminated Ni-eu-Co ores (especially pytrhotite, chalcopyrite, pentlandite) in the vicinity of the Vâ1san Valley (Udubaşa et al., 1988).

-n APU SENI Mts. : .. CODRU .. _ •• 0' __ ' I BIHOR

EAS.T CARPATHIANS

SOUTH CARPATHIANS SUPRAGETIC GETIC LOWER DANUBIAN IUPPER DANUBIAN

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GEOLOGI CAL ,FORMATIONS

1:>.::.'/:J1 c=:J2 [5233 IDTIlIIII4 ~5 .jA,,'',.l'16 IVyVyv l7 ~8 ~9 ~10 ~11

GEN ETI C TYPES

COMMODITIEŞ

"111/12"3 .4 CJS',,6 [.: ::.::-:.17

Fig. 7 - Suggested time distribtition of representative aceumulations of metalliferous and nonmetalliferous mineral resour~ using lithostratigraphic correlation markers of the Proterozoic and Paleozoic formations

(ace. to Ktiiutner inZoubek, 19Ş8; with completions) Key: GEOLOGICAL FORMATIONS: 1, molasse formations; 2, metadetrital rocks; 3, limestones and/or dolomites fonnations; 4, graphite schist formations; 5, leptino-amphibolitic formations; 6, acid volcanic rocks; 7, basic volcanic rocks; 8, granite-granitoide; 9, amphibolites; 10, thyolitic metavolcanics; Il, basic volcano-sedimentary formations. . GENETIC TYPES: 1, hydrothermal; 2, marine; 3, volcano-sedimentary; 4, metamorphosed magmatic liqUid;

5, metamotphosed hydrothermal; 6, metamorphosed volcano-sedimentary; 7, metamorphic; 8, metamorphic differentiation. COMMODITIES: 1) Fe, NI±Cu; Cr. 2) Mn;!:Fe, barite. 3) Cu, Pb, Zn, Py, Au, Ag, barite. 4) U-Th, TR, Zr, Nb, Ta, -Cu, Pb, Zn, Py, Mo, Bi. 5) Muscovite, quartz,feldspar. 6) Li, Be, Kyanite, taIc. 7) Graphite. REPRESENTATIVE ACCUMULATIONS: 1. Palazu Mare (Fe); 2. Armeniş, Valea Fierului-Bouţari (Fe)~ 3. Âltân Tepe (Fe, Cu); 4. Poiana Mărului (Ni); 5. Titianu (Ni); 6. Puskarschi (Cr); 7. Vâlsan (Ni, Cu); 8. Delineşti (Mn); 9. Răzoare (Mn); 10. Bâzdâga (Fe, Cu); 11. Valea Blaznei (Py, Zn, Pb±barite); 12: Grădiştea de Munte (U, Th, Tr, Nb, To); 13. Atpaş <Ee); 14. Porumbaeu (Py, Zn, Pb); 15. Topleţ (Fe); Globu Rău (Mn, Fe); 16. Negovanu (Kyanite); 17. Ungurelaş (Graphite); 18. Muntele Rece (Feldsphar, U); 19-23. Uricani (Quartz), Teregova (Feldspar), Voineasa (Muscovite), Conţu (Li), Pietrele Albe (Be); 24. Boiţa Haţeg (Py, Zn, Pb); 25. Boclugea (Fe); 26. Şipot-Dibarţi' (Cu, Pb, Zn, Fe, barite); 27. lacobeni (Mn); 28. Burloaia-Fundu Moldovei-Leşu Ursului-Bălan (Py, eu. Pb, Zn); 29. Rusaia (Fe); 30. Izvorul Cepii <RY); 31. Teliuc, Ghelar (Fe); 32. Izvoiul Bistriţei (Fe); 33. Lelese (taie); 34. Muncel (pb, Zil), Veţel (Cu, Zn, Pb); 35. Păiuşeni (U, Cu); 36. Highiş (Cu, Py); 37. Muntele Mare (l;J); 38. Balabancea, Măcin (Fe); 39. Zimbrul~ Padiş (U)±Cu, Pb, Zn); 40. Rămuşa(U, Mo); 41.llişova-Gabretina (U, Cu, Pb, Zn); 42.Sviniţa-Streniac (U±Cu, Pb, Zn); 43. Budinic, Ciudanoviţa (U); 44. Repedea (U). .

Băile Bor·Si1J •

6>-

11 - Facies distribution in the Burloaia-Gura Băii district {ace. to Zincenko, Key: 1 - central fades with Pb-Zn bearing massive pyritic ore; 2 - intermediate facies with massive andlor disseminated pyritic ore; 3 - marginal facies with Zn-Cu bearing disseminated bearing dissemÎnated ore; 5 - Neogene volcanic rocks; 6 - underground development.

UPPER PALAEOZOIC METALLOGENESIS .

The Apuseni Mts. are nr~''''",r''rI,h advanced the total resources esl1rnlatt~S

Fe, Cu, Mo, Wilson orogenic

country.

MetaUogenesis related to intracontinental .... " .... "'"

South Carpathians U ores related to H ...... '.p."',lU

23

The products are by Fe-Ba, Pb-Zn (siderite, ankerite, .... v.v.u .. v,

calcite, magnetite, lenlatlte, barite, galena, sphalerite) foundin the Devonian calcareous chlorite-albite and schists of the Ruşchiţa-Alunugreenschists G~elar Series, upr'ag~~tlc N""nnţ'C (Poiana Ruscă South Carpathians). The ores are ofLahn Dill type and the Ghelar-Teliuc district 1977) (Figs. 12, 13).

21

Last but not least, some comme,nts about the Precambrian pegmatites: minor Be and Li~bearing pegmatites are found in the South Carpathians. Spodumene bearing pegmatites found at Conţu, in the Middle Proterozoic Sebeş-Lotru Group of the Getic Nappe, are the most charactenstic. Alternative to the magmatic formation, Hann (1987) estÎmates that pegmatite genesis is a metamorphic process resulting in differential matter mobilization and anatexis through metasomatism.

5 .... ,..----- 5 OUT H o o B ROG E A -----.. ,

o 500 looom ...... -""'-""'"---'----',

Fig. 9 - Cross-section through the northem part of South Dobrogea in the Ovidiu-Palazu-Cocoşu region (ace. ta in Zoubek, 1988).

Key: I Upper Cretaceous and Cenozolc cover; 2 Jurassic carbonate cover; 3 - "Greenschist Formation" (Baltăgeşti Member) (Upper Brioverian); 4-5 - Cocoşu Group (Brioverian): 4 - upper detrital formation; 5 lower spilitic formation; 6 - Palazu Mare banded iron ore formation (Lower Proterozoic); 7 -Gneisses (Archean?)

LOWER P ALAEOZOIC METALLOGENESIS

metallogenesis is characterised by Fe,..Mn, Cu, ·Ba and U deposits related to intracontinental rifting which promoted the cycle. Except the Izvoru Cepii pyrite stratiform ores located in the Ordovician-Silurian Repedea (East Carpathians), metallogenetic products, that might be ascribed to the Caledonian orogeny in the broad sense, are not exposed. Th~ most representative occurrences of the Lower Palaeozoic metallogenesis are linked to Tulgheş Group (East Carpathians). According to and petro­metallogenetic characteristics the interpre\ation of rift related metallogeny (Folea et al., 1987) Îs therefore adopted. J

Carpathian metalliferous occun-ences represent around % of the total resource estimates of Romania. A 180 km long belt' located in the Bucovinian~Subbucovinian nappes runs NW-SE ftom Baia Borşa to Bălan. Mineralizations of Pb-Zn, Cu-pyrite, Fe-Mn and Ba character arerelated to volcapogenic of the Ordovician Tulgheş Group. metalydite (metajaspilite )-graphite assemblage with specific black quartzites exposes lenses Fe-Mn ores (rhodocrosite, rhodonite, tephroite, spessartite, mangangrunerite, and Mn oxides and hydroxides at Câr1ibaba, Iacobeni, Broşteni and of ores at Holdiţa-Broşteni (Bistriţa Mts) (Hârtopanu, 1996). The volcano-sedimentary

22

formation bimodal basic-acid volcanics contains folded and boudip.ed sulphides and stratiform .disseminated sulphides (pyrite, chalcopyrite,

galena and arsenopyrite, locally also cassiterite, bismuthinite, boumonitey

tetrahedrite) (Kiâutner,1966. 1984,1988, 1989). Theores are found in four metallogenetic districts, Borşa-Vişeu (Maramureş) (Figs. 10, 11), Fundu Moldovei-Leşu Ursului, Şumuleu and Bălan-F~gu Cetăţii.

Gura III. Hlil

ssv

• • • * "" * • • ~ . . .. . . .. . ~ . . . . . . . .. . ~ . .

NNE

. . . . .. ~ . . . . . . . . ~ ~ . ~ . ~ . ~ . . 11·oooj 2

IQ,-Geological cross-section through the Gura Băii,ore deposit (ace. to Zincenco et a!., 1975). Key: l·y Dealul Bucăţii rhyodacitic metavolcanics; 2 - Dealul Bucăţii base-metal lt.wel; 3 - lower phyJlîtic graphiiici~hists; 4 - Burloaia-Gura Băii lower rhy~itic me!avolcanics; 5 - lower phyUitic muscovitic schists; 6 - impregnation and massive-looking base-metal gre:from Burloaia-Gura Băii Ieve1; 7 upper phyUitic 8 - Burloaia-Gura BăU Upper rhyodacitic metavolcanics; 9 - upper phyllitic 10 - muscovitic-quartzitic schists (Ivăşcoaia 11 - neogene andesites; 12 - faults.

Krautner (1984) divided ores into morphologic-depositional types: - Isipoaia type: massive sulphide lenses with inner metal character outer

Cu-pyrite mineralization and peripheral pyrite halo Burloaia, Gura Băii, Colbu, Ursului zone II, Fundu Moldovei zone 1); .

- Fundu Moldovei type: ştratiform dissemÎnated Cu-pyrite as ore-bearing beds (e.g. Fundu Moldovei zones II and In, Ursului zone III);

Ursului base metal ore grading to Pb-Zn Leşu zone 1) or Cu (e.g. Bălan) disseminatro,ns. Ore are found in places as a result of metamorphic mobilisation Bălan).

Less extended similar Cambrian occurrences are found elsewhere, in the South Carpathians (stratabound pyrite, sphalerite, galena, chalcopyrite, 'bomite ores at Boiţa Haţeg, Gtoup Getic Nappe) and in the North Apuseni Mts. (small-sized concordant and Cu-pyrite ores at Lupşa, Muncel Nappe of the Gilău-Muntele Mşre Massif).· .

23

Fig. Il - Facies distribution in the Burloaia-Gura Băii district (ace. to Zincenko, 1975). Key: 1 - central facies with Pb-Zn bearing massive pyritic ore; 2 - intermediate facies with Cu-Po-Zn bearing massive andlor disseminated pyritic ore; 3 - marginal facies with Zn-Cu bearing disseminated pyritic ore; 4 - Cu­bearing disseminated pyritic ore; 5 - Neogene volcanic rocks; 6 - underground development.

UPPER PALAEOZOIC MET ALLOGENESIS .

The basement nappes and the Pennian molasse of the South Carpathians and Apuseni Mts. are preferential sites of Fe, Cu, Mo, Pb-Zn and U ores related to incipient and advanced stages of a Variscan Wilson orogenic cyc1e. Such occurrences represent only 2 % of the total resources estimates of the country.

Metallogenesis related to intracontinental rifting

The products are represented by Fe-Ba, Pb-Zn lenses (siderite, ankerite, dolomite, calci te, magnetite, hematite, barite, galena, sphalerite) found in the Devonian ca1careous chlorite-albite and sericite-chlorlte schists of the Ruşchiţa-Alunugreenschists fonnation, Ghelar Series, Supragetic Nappes (Poiana Ruscă massif of the South Carpathians). The ores are of Lahn Dill type and c1uster in the Ghelar-Teliuc district (Kdiutner, 1977) (Figs. 12,. 13).

24

Fig. 12 M Poiana Rusc! Hercynian crystaHine massif - South 1 Padeş Series (Upper Devonian - Lower Carboniferous); 2 M .Io.&l.l:ll!ll;;M'v~;lRill)l

• Muncel·VeţeI type base·metal accumulations; 4· basic volcano-sedimentary fOl'lrnation metatuff deposlts; 6 • iron ore in earbonate and oxidic 7 M schists

8 • Paleocene gtanitoids.

o SO 100 150m ti. t

300

200

100

~11

Fig. 13 - Geological section tlrrough the Teliuc ore deposit (ace. to Krliutner, 1970). I • alluvia; 2 • gypsum mafks; 3 • quartzites; 4 • chalybite; 5 . iron dolomite; 6 • dolomites within the ore

deposit; 7 • lin1onite; 8 • itabirite, magnetite; 9· m11estones; 10· dolomites; 11 - chlorite-sericite and chlorite -calcareoua bearing tuffite.

Metallogenesis 10, su~~uction ... related settings

The Carboniferous Pad,es series with related ores occurs in the north-eastem part of the Poiana Ruscă massif (SouthCarpathians) andthe Rapolt massif (Apuseni Mts) (Krăutner, 1964). The Muncelu Mic-Rapolt district contains Pb-Zn-Cu stratiform banded and disseminated ores p~ly mobilised along schistosity; the host rock is acidic metavolcanic part of the Leşnic fonnation (upper part of the Padeş series) (Gurău, 1967, 1980). Muncelu Mic deposit is of Pb ... Zn character (Pb/Zn = 1/2}and Veţel deposit of Zn-Cu character (Zn/Cu = 2/1). ;

Metallogenesis in post .. coUision related settings

In Permian molasse environments stratiform Cu-U and discordant Cu-Mo mobilisates , .'

occur in sandstone-microconglomeate levels at Zimbru and Cu stockworks and U vein-like ores in rhyolites at Rănuşa, in the Moma massif (North Apuseni Mts) (Vlad, 1980). ores consist of pitchblende, chalcopyrite, umohoite, bomite, calcite, covellite,' tetrahedrite, molybdenite and pyrite in quartzose gangue and belong to an ensialic aborted' Simtim. Cu-U ores found at Ciudanovita, South Banat region (South Carpathians) .

ALPINE MET ALLOGENESIS . ,

fi'" . ~.

. The Alpine melallogenesis characterised especially by Au, Ag, Pb, Cu, Mo, Mn, (± Ti,. V, W, Sb, Bi, Cd, Hg, Ca, CrltNi, U, Th, Tr) is, significantly developed throughout

the mobile' zones ofthe Romanian territorY'(Carpathians andNorth Dobrogea). Metallogenesis related to an stages of a Wilson otogeniccycle has recognized,

Le.from intracontinental rifting to spreading-, subduction-, co.lIision- and post-collision­related settings. The geological features that controlled the episodic ore deposition during this cycle are correlated with the geochemical behaviour of themaj6r metals (Plate 1) .. The main stages are COl"Jlected with the Laramian (Banatitic) magm.atic products (especially skam deposits and' porphyry deposits) and Late Tertiary volcariicproduct (especially ve in deposits and porphyry deposits). .,,~ .

Most important metallogenetic areas are moreover\ coincidental with plutonic spatial disposition, especially with the subvolcanic structures, much more obious in case of Tertiary magmatism (Fig. 14). Highly significant' the fracture set connected to pluton, its evolution controlling the metallogenetic events.

Such genetic relationships, present well specified by adequate means of geological and geophysical studies, have been promoted in the Metaliferi Mountains (Ghiţulescu, 1935) and to a large extent geophysically proved in the volcanic zones of the East Carpathians and in thewestem part of the South Carpathians, in the banatitic province (Socolescu et al., 1964; Socolescu, 1972, respectively).

\

26

MetaDogenesis related to intracontinentaI rifting

The products of this metallogen~tic acţivity are found both in the Carpathian and the North Dobrogean realms. ' (

The Dobrogea well expressed NW -SE trending alignments of bimodal (basaltic) rhyolitic igneous rocks are especially associated with stratabound Ba-Pb-Zn and Fe ores within Spathian calcareous-terrigenous turbidites of the Tulcea tectonic ' unit (Vlad, 1978).

~s

-' ~7

-'a c::? '

. ~..,;) 10 ,,-...... ": :::: ....... "

o 10 10 lOk .. , Il . • .

- ' . ' . . .

Fig. 14 - Alpine magmatic concealed structures, deduced from geophysical data

B~~OY

. . (acc. to Andrei et al., in: Vlad, B<;>rcQş, 1994). \ .

Key: 1- Neogene volcanics; 2 - Upper Cretaceous-Paleogene magmatites; 3 - isl~d arc products - andesites and basalts, Upper Jurassic-Lower Cretaceous in age; 4 - Jurassicophiolites; 5 - JuraSsic alkaline intrusions; 6 - fault; 7 - inverse fault; 8 - nappes; 9 x - plutons and Neogene intrusi ve bodies; 10 x - plutons and intrusive bodies, Upper Cretaceous-Paleocene in age; Il x -plutons and intrusive bodies, Upper Jurassic-Lower Cretaceous in age~ 12 ~ - Jurassic alkaline intrusions; 13 x - deep-seated extend of the ophiolitic complex; 14 x - major fractures (x = Geophysical elements)

27

In the Somova-Cortelu area stratiform sedimentary barite with subjacent Pb-Zn ores formed inside minor submarine depressiens; subsequent small-sized Ba-Pb-Zn veins occurred in steep-dipping fractures .a.long antic line cres~ and stockworks K-altered rhyelites. margin of ilie North Dobrogea rrfassic contamsinfiltration of Rîo Marina type within some Spathian turbidites at Iulia. The skam deposits contam hematite­magnetite as a result of Fe mobilişation trom the basement. Otber details conceming the geology and the mineralogy of these types of ore deposits in lanovici et aL (1957, 1977), Vlad (1978).

Danubian units of the South Carpathians contain Mo-W mineralization the Mraconia regioo.. The enviroiunent consists of bimodal magmatic prQducts represented by . north-south monzogranite-granodiorite dykes and lamprophyre dykes that penetrated mylonitised metamorphic rocks ofthe Neamţu series (Metallogenetic unit IA in Plate 1). A major monzogranite dyke underwent potassie and phyllie alteration; molybdenite and common sulphides veinlets and impregnations occur in the phyllie zone. .carbonate Întercalations of the surrounding crystalline schists were converted into skams with scheeHte, pyrite, chalcopyrite, magnetite andhematite. Radiometrie age data (209-145 m.y., and bimodal magmatic pi'oducts with associated porphyry Mo mineralizatiofi are characteristic of an aborted ensialic rift.,!t ls, however,difflcult to ascertain trus rifting represents back-arc extension of Paleozoie collisional Ogradena granitoids or incipient intracontinental rupturing during the Early Mesozoic (Vlad et1984).

. basement nappes ofthe South aud EastCarpatruans contain small Pb-Zn-Ba ore . deposits. Făgăraş Group (South Carpathians) is cut by Jurassic bimodal (alkali-rhyolite and lamprophyre) dykes and Pb-Zn ore veins controlled by regional ENE-WSW lineation. Common sulphides occur in quartz or barite gangue (Bârsa Şinca-Holbav

metaliogenetÎc districts) (Manilici, 1956; Nedelcu, Anton, 1964). Aborted rifts found in the Bucovinian Nappe (East Carpathians) contain Ba-Pb-Zn, and Mo oceurrences related to MesozoÎc sedimentary and igneous rocks, as explained below (Ianovici, Borcoş, 1983).

TriassÎc dolomitic limeston~s at Delniţa contain stratabound Fe (siderite) ores assoeiated with minor barite and Pb-Zn ores. The lens-like bodies are mainly sideritic­ankeritic in the east hematitie in the west (Tănăsescu, Pitulea, 1962; lanovici et aL, 1963).

Along the Ostra-Gemenea-SIătioara alignment. barite and witheri~e accumulations are associated with base-metal ores. At Ostra north-south striking veins cut the metamorphic basement and the Mesozoic sedimentary cover. At least two barite generations have recognized as well as witherite, pyrite, sphalerite, tetrahedrite; at depth the penetrated gneisses are impregnated with barite. It seems likely that early barite occurrences were remobilised during post-Jurassic rifting, before major Middle Cretaceous deformation. mineralization is found diseontinuously as as Slătioara where base-metal and barite veins cut the schists (Metallogenetic Unit 1 B in Plate 1).

,The Jurassie-Lower Cretaceous (196-121 m.y.) alkaline intrus ion that occurs at Ditrău exhibits a conspÎcuous zonal structure; inner foidites are surrounded by syenite and monzonite. Homblendite, diorite, and alkali-granite o,ccurrenccs are peripheral. Numerous lamprophyre, m'icrosyenite, alkali-granite aud aplite dykes cut the massif. Albitite segregations and carbonate occur locally. Porphyry Mo-like mineralization oecurs alqng east-west alignments, especially in the east at Aurora. The

28

ores are at Jolotca hosted by diorite and homblendite and contain common sulphides aud subordinate ilmeno-rutile. ilmenite. tapiolite, columbite. The veins cutting the ,,,r.,,,nn .. contain xenotime, common sulphides and niobo-tantalates (Ianovici, 1938; Codarcea et 1958; Ianovici, Ionescu, 1964; Constantinescu et al., 1983; Jakab. 1998) (Metallogenetic Unit 1 C Plate 1).

Metallogenesis related to ocean floor spreading

The Nappe of the South Carpathians contains ophiolites related Cu ores. During Mesozoic times an elongated with oceanic crust formed between the Getic and Danubian realms named by Rădulescu and Săndulescu, 1973); it corresponds to the above-mentioned rift of East and South Carpathians. The resulting basaltic flows and pyroclastic rocks associated with . Lower Cretaceous flysch "' ........ u .. " ... " of Severin Nappe were obducted eastward during Laramian compression when

Getic and the Danubian realms collided. Cioflica et al. (1981) provided geological and geochemical evidence that the ophiolite association formed as tholeiitic ocean-floor in a small ocean basin; the re1ated ore deposits at Baia de Aramă, were ascribed ta the Joma type sensu Pearce and (1977). They oeeur basalts as smaIl stratiform pods of massive chalcopyrite, with subordinate pyrite and sphalerite quartz gangue (Savu et al., 1986).

ore 1S commonly underlain by pyrite + chalcopyrite + sphalerite stockworks (Metallogenetic Unit 2 Plate 1).

MetaUogenesis in subduction-related settings

Three successive Alpine subduction events in the Romanian Carpathians gave to vast of metallic ore deposits in Romania.

Jurassic-Lcwer CretaCeous. Upper Cretaceous-Paleocene.and Tertiary events in turn ore of isiand arc or types (Plate 1).

The JUl'llSsic-Lower Cl'etaceollS subduction yielded three stages of magmatism the South Mts 15). These are a tholeiite series and subsequent "'''''''''-UJLftUJlU''''

both arc type, and a spilitic complexassoci~ted with an active marginal basin (Nicolae et al., 1992). .

metallogenesis related to the tholeiitic consists of Fe-Ti-V and Ni late-magmatic segregations in gabbraieintrusions and pyritic veins and in basaltic

(Socolescu. 1940; 1972; Cioflica. Vlad, 1984). The Fe-Ti-V are found as titanomagnetite + ilmenite lenses grains within layered gabbroic bodies at Căzăneşti-Ciungani. Ni ores are confined to the Ciungani gabbroic body 'illJ","""'''''' pyrrhotite and pentlandite with associated ehalcopyrite magnetite oceur as a small pod. The pyritic Cu ,volcanogenic ores are of type sensu and Gale (1977). Various and stockworks are controlled by brecciated basalts at Căzăneşti-

•.• ..u~; ...... JlL, Almăşel, and Nouă (Socolescu, 1 Savu, 1972). The mineralization at Pătârş iS located in theupper part of a basaltic unit and contains an inner with pyrite + chalcopyrite veinlets and a massÎve pod, surrounded by a disseminated pyrite aureole (Vlad et al., 1998).

1r.:-:-l l...:....:.....

sF---j 2~ 3rvvv1 u....:u 6r;>:j 71+ .. +;1

4~ 8~

9- 10- 11-12C--

13 C:--:) 14C:::::> 15~~:) 16~ 17 c:::> 1- V

r

..... -:.:.-.':.:.1, ... .::.,

':~::=~=========~==-~---------

Fig. 15 - Ophiolites and island arc products in the alpine structural setting ofthe central-westem part ofthe Southem Apuseni Mountains (ace. to Andrei et al., 1986). Key: 1 - Neogene molasse; 2 - Neogene volcanics; 3 - Upper Cretaceous-Paleocene volcanics; 4 - Jurassic sedimentary formations; 5 - Cretaceous sedimentary formation; 6 - Upper Jurassic-Lower Cretaceous islao.d arc products - andesite, basalt, 7 - diorite-granodiorite; 8 - Jurassic ophiolites, gabbros with Fe, Ti, V b); 9 -Fault; 10 - Nappe; Il - Valea Muresului transcrustal fracture; 12 x. - Sheeted-dyke complex; 13 x - Gabbro-diorite intrusions Jurassic in age; 14 x - Granodiorite intrusions Lower Cretaceous in age; 15 x - Quartz-diorite intrusions Paleocene in age; 16 x - Fe-Mn prospective area (1. Soimut-buceava, II. Pamesti); 17 x - Base­metal prospective area (II.Vorta-Dealul Mare, Ill. Savarsin, IV. Cerbia, 1. C8zanesti-Rosia).

IV -o

30

The calc-alkaline . contain base-metal ores Vorta. dacitic-andesiticrocks andrelated pyroclastics underwent strong silieifieation aqd argiUization. The altered bimodal volcanies striking lenses and impregnations pyrite, sphalerite, galena and chaleopyrite and itwas thought that the ores are Kuroko type (Udubasa et 1970, unpubI. data). Vlad (1984), Vlad al. (1998) took over !hat sueh an island arc suite of roeks may incorporate· Kuroko-porphyry eOt:liDer

Minor voleano-sedimentary Mn ores. associated with jaspers oeeur in Lower Cretaeeous sediments at Şoimuş-Bueeava, Pârneşti and Godineşti (Soeolescu, 1940; Savu, 1972).

This arc-related metallogenesis Is represented in 1, Metallogenetie Unit 3.

The Upper C,.etaceous-Paleocene widesp,.ead weshfard subduction gave to polyphase calc-alkaline magmatism (Laramian magmatism, also known as "Banatitic"). This magmatic belt is 280krn long in Romania, and TUnS from Apuseni Mts, in North, to the 80uth Carpathians. It extends further southwards in Eastem Serbia (Yugoslavia) and further to Srednagora (Bulgaria) (Ciofliea, Vlad, 1980). major intrusive event, eommonly with a monzoruorite or diorite-granodiorite evolutionary trend ora granodiorite-granite evolutionary trend or both, i8 metallogenetieally the most important. .. The magrhatîsm the monzodiorite or diorite-granoruorite was generaUy relatedto eopper mineralization in porphyry environment. The magmatism of granodiorite-granite type generally

ores non-porphyryenvironment: skam deposits predo~nim:ite, whereas vein deposits are rare.

In Romania, the Laramian or Banatitic belt is comprised between the North Apuseni, South Apuseni and South Carpathian subbelts. subdivisions result from different subduetion-related settings; ihey are at present distributeq along. a major lineation.

metallogenetie unit is enaraeterized by granodiorite-granite ma~grrlatl.sm PO;:l"l1"P~lrI base-metal metallogenesis (Metallogenetie Unit 4a in Plate ~,

metallogenetie zones have been recognized (Ciofliea, Vlad, 1984): 1) inner zone eorresponding to a northwestward direction of subduction exhibits

a complex metallogenesis in the Bihor-Gilău Mts. It contains Fe, Mo, Bi, W, Cu, U, Ni, Pb, B, Au and Ag ores in. skams, stratiform-impregnation bodies, and veins in the Băişoara (lazăr, Intorsureanu, 1982), Bihorului (Giuşcă, 194 î; Stoici, 1 1983) and Luncşoara-Brusturi-Poiana rustriets (Berbeleac, Ionesc~ 1 Giuşcă 'et al., 1976; Lazăr et al., 1978). Băiţa Bihorului is the most important Theore zoning around the pluton is Mo-Bi-W-Cu-U-Pb-Zn/Mo-Bi-W-Cu-U-Pb-Zn-B and is expressed ina vertical eolumn extending up to 1.5 km away from the granite pluton. Calcie and magnesian skams contain

. molybdenite, bisinuthinite, sulfosalts and scheelite (three generations), Cu minerals, galena, sphalerite, szaibelyite + luc,lwigite, fluoborite and kotoite. Metasomatised detrital homfeis (epidote + chlorite + actinolite, albite +, quartz sericite + quartz associations) contain and Cu stratabound lenses and molybdenite in impregnations and veinlets, whereas Paleozoic detrital rocks and crystalline schists situated from pluton enclose bands veins of common sulphides ores. same granitie intrusion yielded

3\

t:=Js 1= ..... j10 """" 11 Zt

Fig. 16 - Upper Cretaceous-Paleocene magmatism and metallogenesis in the Alpine structural setting ofthe Apuseni Mts region (ace. to Borcoş, Andrei et al ., 1994; Borcoş etal., 1994). .

Key: 1 - Tertiary molasse; 2 -Paleogene epicontinental formations; 3 - Mesozoic sedimentary cover; 4 - Permian molasse; 5 - Metamorphic formations: a - granitoids; 6 - Neogene volcanics;7* - granite-granodiorite complex: dacites, andesites; 8* -quartz-diorites; 9* - andesite-quartz andesites; 10 - rhyodacitic volcano-sedimentary formation, Upper Cretaceous-in age; II - Mesozoic ophiolites; 12 x - pluton; 13 x ~ intrusi ve major structures with their culminations; 14. x - intrusive structures of . intermediary composition; 15 - tectonomagmatic and metallogenic alignments; 16 - fault; 17 - inverse fault; 18 - nappes; 19 -main aceumulations (1-19 denominations); 20 - occurrences; 21 - d istricts. Denominations ofthe accumulatÎOns: l - Juleşti-Valea Fagului; 2 - Valea Seacă; 3 - . Băiţa Bihor; 4 - IzvOl;ul Bihorului; 5 - Valea Titişor; 6 - Valea Vacii; 7 -Brusturi-Luncşoara; 8 - Râul Mic; 9 - IivQrul Anieşului ; 10 - Gruiul Dumii; II - Liţa; 12 - Masca; 13 - Nyerghes; 14 -Cacova; 15 - Sohodol; 16 - Budureasa; 17 - Valea Boaica, Valea Stanciultii; 18 - Răchiţele; 19 - Borod-Comiţel.

* 7-9 Intrusions Paleocene in age x Geophysical elements

32

"pentametallicll (U, at Avram Iancu

Ni, Co, Bi) ores veins and replacement base-metal ores at

ores as stratifonn impregnations and Luncşoara (Lazăr et al.,

1980). 2) the outer zone (for the same subduction is noted for

located in the VIădeasa Massif. Hydrothennal Pb-Zn 6res occur metals and

Scrind-Răchiţele

(Berbeleac lJ'~n~1tp et . Gheorghiţescu 1980) Borod-Comitei al.,1982).

Some further details conceming the regional zoning in the area are given by Ştefan al. (1988).

South Apuseni subbelt

In a _area are by or granodiorite magmatism with caldc Fe-skam (Vaţa) granodiorite-granite magmatism with Mo-Cu-pyrite vein deposits (Săvârşin, Cerbia). Recent radiometric age data "' ... /<,.1<, .... ;,., that tms magmatism may be of Lower Cretaceous age (Ştefan, 1986). The plutonism would represent the completion ofthe above-mentioned subduction event.

Carpathian (Banat-Poiana Mts) subbelt

This unit oftwo zones that are paraNel to a suture-like.contact between two blocks that collided during the defonnation (Vlad, 1979). suture is the

remnant of the above-mentioned rift of the East and South Carpathians (Meta110genetic Unit 4b in Plate 1, 1 magmatic bodies to the activity are

illustrated in outlined geophysical images et al., 1994) 1) the zone (for a westward direction of subduction) in the South Banat Mts a monzodiorite or diorite-granodiorite magmatism and related Cu-Mo porphyries that

occur at Moldova Nouă (e.g·, Suvorov orebody, Gheorghiţă, 1975) and Sasca (Con~tantinescu, 1980);

2) the outer zone in the North Banat-Poiana Mts exposes granodiorite-granite ma;grI1latlSm with Pb-Zn skarn deposits (Dognecea an4-'Ocna deand Mo-W-Cu

deposits (Oraviţa) (Codarcea, 1931; Vlad, Gherghiţescu, 1975). Regional

occurrences, tectonic characteristics, alteration and L.v ..... j!'" ore mineralogy and other related elements fonn the outline of the metallogenetic models porphyry and non-porphyry environments (Vlad, 1996) (plate I). ~ ___________________ w. _____________________________ ~ _______________ h _________________________________________ _

17 - Upper Cretaceous-Paleocene magmatism and metallogenesis in the structural ofthe West Meridional Carpatbians to Andrei et al., 1989).

1 - Neogene molllSse; 2 - Mesozoic sedimentary cover; 3 - Pennian molllSse; 4 - metamorphic a) granitoids, b) bllSic and ultrabllSic 5 Upper Cretaceous volcano-sedimentary fonnation a), Upper Cretaceous volcanics b); 6.

granodiorites, andesites; 7 - granites-granodiorites; 8 - monzodiorites-monzogranites; 9 - gabbros-monzogabbros; 11 • inverse fault; 12 nappe; 13 - overthrust plane; 14 - pluton; 15 - pluton culminations of acid composition; 16 .

• pluton culminations ofintennediary and bllSic composition; 17 - main ore (1. Ruşchita, 2. 3. VaJişoara, 4. 5. Ocna de 6. Dognecea, 7. Surduc, 8. Oravita, 9. 10. SlISca MontaJlă, 11. Moldova NouA-.... ",."",,,,,. 12. Moldova Nouă; 13. Vărad; 14. Mare; 15. 18 - districts: 1. ''''''''''''\4, II.Tâncova, III. Ocna de Fier-Dognecea, IV. V. Moldova VI. Lilieci-Nasovl!.l:, VII. Teregova-

a a ~11:.-=12~3~4 ~5!A 1\16 ~ b b

+"'''+11, (. -"15 ::····""}16 . 1 ,+.... ...._" ...... .

c:::> 18 I

O 50 100' lS0km I I ' . !

Nouă

A

Barite

Cu PbZn±Mo .... "-+~+~ _.- ..

.. -. + 55 miI. y ...... .. +

/\. /\ /\ /\ /\

/\ -;:/\ -;:. 75 miI. y XXXlC.

__ .II!Fe±Ti,V lCX)(X

x x X x x)( x

Fi .17

33

34

TABLE 1 - Model Suvorov-Granodiorite Type, Cu-Mo Monoascendent Evolution, Skarn Halo (M IV in Fig. 18A, Plate 1)

DESCRIPTION. Chalcopyrite + pyrite in stockwork in hydrothennaHy altered hypabyssal-subvolcanic intrusives and in rdated skam with retrograde alteration.

GEOLOGICAL ENVIRONMENT . Rock types. Monzodiorite and diorite to granodiorite plutons with hypabyssal­

subvolcanic apophyses intruding carbonate rocks or calcareous siliciclastic sequences of Mesozoic age. The sedimentary rocks belong to the Getic Nappe and the igneous rocks to the Banatitic belt developed in the Apuseni Mts:, Banat-Poiana Rusca Mts., Eastem Serbia and Srednagora. .

Age 72-67 m.y. Structural type. The porphyry copper system is centered on subvolcanic apophyses

of deep-seated plut(ms. . Depositional environment. Deep-seated intrusion of N-S striking and westward

dipping tongue-Iike pluton in mainly carbonate milieu. Intense fracturing: first order strikes N-S and second order strikes E-W (orthogonal system). Permeable volcano­plutonic complex with volcanic part eroded and subvolcanic hypabyssal apophyses exposed.

Major tectonic setting. Andean-type magmatic arc. Large scale zonality/associated deposit types. Cu-Mo sotckwork in hydrothennally

altered igneous host - skam Cu ± Mo, W - replacement Pb-Zn -" telethermal As-Sb -presumable Carlin gold.

DEPOSIT DESCRIPTION Mineralogy. Magnetite ± chalcopyrite, pyrite impregnations in potassic zone,

pyrite + chalcopyrite ± sphalerite, molybdenite, tetrahedrite veinlets and pyrite + chalcopyrite impregnations in 'phyllic zone (restricted areas of intensive silicification contain molybdenite ± pyrite, c~alcopyrite veinlets and impregnations). Magnetite that replaced andraditic gamet and pyrite + chalcopyrite veinlets and impregnations in skam with extensÎve fracturing and propy,litization.

Alteration. Pervasive potassic alteration (biotite + K feldspar + anhydrite) in the lower part of the subvolcanic apophyses is associated with a.ndraditic gamet in carbonate rocks. Phyllic alteration (seri cite + quartz + chlorite) in the upper part of the subvolcanic apophyses is associated with argillic (montmorillonite ± kaolinite) and propylitic (epidote + chlorite + calcite) alteration in skam. The alteration pattern Îs concentric' of Lowell and Guilbert type.

Ore controls. Intense stockwork veining in igneous and skam rocks contains most ofthe copper.

Weathering. Argillization and "Iimonitization". Geochemical signature. Cu, Mo, Pb, Zn, As (Sb, Au, W) Deposits/Prospects Moldova Nouă: Vlirad, Garana, Valea Mare, Suvorov,

Corcana-Baies, Greci-Apele Albe), Sasca, Şopot (Lilieci, Purcariu, Nasovat). :

TABLE 2 - Model Bozovici-Granodiorite Type, Cu-Mo Monoascendent Evolution, Pyrite Halo (M V in Fig. 18B, Plate 1)

DESCRIPTION. Stockwork vein1ets of quartz, chalcopyrite, pyrite and molybdenite in porphyritic intrusion.

GEOLOGICAL ENVIRONMENT Rock types. Minor quartz diorite to quartz monzodiorite apophyses of deep-seated

plutons intruding crystalline of Pre-Mesozoic age. The metamorphic rocks belong to the Nappe and the igneous rocks to the Banatitic belt developed in Apuseni Mts., Banat - Poiana Rusca Mts., Eastern Serbia and Srednagora

Age. "Laramian" Structural type. High-Ievel porphyry subvolcanic-hypabissal apophyses and dikes.

The porphyry copper system not weH expressed. Depositional environment. Deep-seated intrusion N-S striking plutons in

crystaHine schists and shallow (subvolcaruc-hypabyssal) apophyses. Major tectonic Andean-type arc. Large zonalityl associated deposit types. Not expressed. DEPOSIT DESCRIPTION Mineralogy. Quartz with chalcopyrite, pyrite, magnetite and molybdenite

In the upper part of the potassic zone and sporadic molybdenite, chalcopyrite and magnetite impregnation the lower part of the potassic zone (Bozovici). Pyrite ± chalcopyrite, magnetite impregnations in phyllic and argillic zone (Teregova-Lapusnicel). Disseminated pyrite halo.

Alteration. potassic alteration (biotitization) at Bozovici, potassic, phyllic and argiHic alterations at Teregova-Lapusnicel. The alteration pattern is not weB expressed.

Ore controls. Veinlets and mineralized fissures in the upper part. The stockwork pattern is replaced at depth by impregnations (Bozovici).

Weathering. Not weU expressed. Geochemical signature. Cu, Mo, Pb, Zn DepositlProspects. Bozovici, T eregova-Lăpuşnicel

35

Metallogenetic models in porphyry environment. The South subbelt nt ......... tI·" ... " deposits and prospects that have in comrnon the occurrence of porphyritic

tongue-like apophyses of deeply buried plutons of monzodiorite or to granodiorite composition. Such apical centres of hydrothermally developed sulphide mineralization and rock alteration controlled intensively fractured host Two models are outlined, that is Suvorov model with and Bozovici model (Vlad ano Borcos, 1996). Their are presented in 1, 2 18.

36

w

+ + + +

+ + +

+ +

1 1......· ...... 1 21 '--_------II

A

+ +

41 + + I slx

Fig. 18 - Banatitic porphyry copper models (ace. to Vlad, Borcoş, 1996).

B

E

7l:·:1M a b

Key: A. Model Suvorov; B. Model Bozovici. 1 - Supragetic crystalline schists; 2 - Getic crystalline schists; 3 -carbonate rocks; 4 - monzodiorite and diorite to granodiorite plutons; 5 - subvolcanic and hypabissal apophyses of dioritic to granodioritic composition; 6 - volcanic edifices of andesitic composition; 7 - mineralization: a) porphyry copper; b) Cu skam.

Fig. 19 - Banatitic skam models (ace. to Vlad, 1990). Key: 1 - granitoid pluton; 2 - dyke; 3 - Model Băiţa Bihoru1ui; 4 - Model Ocna de Fier; 5 - Model Dognecea.

... ,." .... .tM.J 3 - Model de Fier: Fe-Cu Skarn Deposits (M II in Fig. 19, Plate 1)

DESCR1PTION. Magnetite + hematite, chalcopyrite + pyrite in crudc dar:k and in magnesian skams.

GEOLOGICAL ENVIRONMENT Rock types. Granodiorite pluton intruding carbonate rocks. The carbonate

belong to Supragetic nappe and to the Transylvanide and Apusenide Groups of Nappes. The plutons belong to the Banatitic belt developed in the Apuseni Mts., Banat­Poiana Rusca Mts., Eastern Serbia and Srednagora.

Age. "Laramian" Structural type. The skarn association occurs near the contact by

ditfusion/infiltration metasomatism (proximal skarns). Depositional environment. Crystruline schists and sedimentary carbonate rocks

intruded by felsic plutons. Major tectonic Andean-type or island arc subduction-related magmatism. Large sca1e zona1ity/associated deposit types. Contact aureole around the pluton:

Fe-Cu skarn -- Pb/Zn skarn -- polymetaJlic replacement or pyrite veins. DEPOSIT DESCR1PTION Mineralogy. Magnetite + hematite ± ludwigite, pyrite, chalcopyrite, sphalerite,

galena. minerals may be present. A1teration. Dolomitic environment: grossularite + vesuvianite inner zone; diopside

+ phlogopite center; forsterite ± phlogopite, clinohumite outer cruciphyre peripheral zone. Retrograde alteration to tremolite, epidote, serpentine, truc. In places temperature fassaite, spinel

Crucareous environment: andradite in zone~ pyroxene restricted outer zone; marble peripherru zone. Epidote, chlorite, tremolite-actinolite as post-skarn minerals. In places

temperature spurrite and melilite (Magureaua Vatei). Igneous rocks may be altered to diopside + grossularite (endoskarn).

/

Ore controls. Irregular or tabular iron oxides bodies in andradite skam or fractures zones in marble. Magnetite + ludwigite magnesian skams. Associated rocks are barren.

Weathering. Fe-rich gossan. . Geochemical signature. Cu, Zn, Co, Bi. Strong magnetic anomalies. Deposits: Ocna de Fier, Băişoara, Măgureaua Vaţei, Tincova.

37

Metallogenetic models in non-porphyry environment. Apuseni Mts and South Carpathian subbelts contain skam deposits and prospects related to granodiorite - granite plutons. When wall-rocks are mainly deposits occur near contact and skarn deposits occur contact. When wall-rocks are various sedimentary rocks and coeval.or older igneous rocks, magnesian and calcic skams with Mo, W, Bi, Cu, Pb, Zn B are found near and away the pluton.

38

models are defined that is the Ocna de model and the Dognecea model of host rock with proximal~and distal skarn formation, respectively, and

8ihorului model with formation through the contact of the pluton. These contrasts are the re suIt processes that proceed to different extent in response to similar magmatism and wall-rocks of various origin. Tables 3, 4, 5 Figure 19 show their

TABLE 4 - Model Dognecea: Pb-Zn Surn Deposits (M III in 19, Plate 1)

DESCRlPTION. Sphalerite + galena in dark calcic skarns. GEOLOGICAL ENVIRONMENT Rock Granodiorite pluton intruding rocks. carbonate rocks

belong to the Supragetic Nappe and to Transylvanide and North Apusenide Groups of Nappes. The plutons belong to the Banatitic belt developed in the Apuseni Mts., Banat-Poiana Mts., Serbia and Srednagora.

«Laramian" Structural type. skarn system occurs hundreds of meters from intrusive by

infiltration metasomatism (distal skarns). Depositional environment. CrystaHine schists and sedimentary carbonate rocks

intrucled by feisic plutons. Major tectonic setting. Andean-type or island arc subduction-related magmatism. Large scale zonality/associated deposit types. Contact aureole around the pluton:

skarn -- Pb/Zn -- polymetaJlic replacement or pyrite veÎns. DEPOSIT DESCRIPTION Mineralogy. SphaJerite + galena + pyrite ± magnetite, chalcopyrite, arsenopyrite,

pyrrhotite. Alteration. Andradite restricted inner Mn-salite to Mn-ferrosalite (Fe-

diopside) center; Mn-hedenbergite outer zone; marble peripheraJ zone. Retrograde to tremolite-actinolite, chlonte, epidote, ilvaite.

Ore controls. l'v1n-hedenbergite ± ilvite skarn contruns pipe-like or tabular Pb-Zn orebodies.

Weathering. with strong Mn oxide struns. Geochemical signature. Zn, Pb, Mn, Cu, Deposits: Dognecea, Ruschiţa, Brustun.

ore deposits have mined pre-Roman and in the century by such well-known geologists (from the Freiberg school) as B. von Cotta and F.

Accordingly, the deposits at Dognecea, Ocna de Băiţa 8ihorului became ali over world. have a rich complex paragenesis, with up to 200 ore and

gangue minerals. Several minerals were described from deposits first time, ludwigite, szaibelyite, veszelyite..etc., Udubaşa et al. (1992).

TABLE 5 - Model Baita Bihorului: Mo-Bi-W-Cu Surn Deposits (M I in Fig. 19, Plate 1)

DESCRIPTION. Molybdenite, scheelite, chalcopyrite,' Bi-minerals in caldc light skams and magnesian skams.

GEOLOGICAL ENVIRONMENT Rock type. Granite (granodionte) pluton (batholith) intruding carbonate rocks and

earbonate-siliciclastic sequences. The earbonate roeks belong to the Getic Nappe andthe Apusenide Group of Nappes. The plutons belong to the Banatitic belt developed in the Apuseni Mts., Banat-Poiana Rusea Mts., Eastem Serbia and Srednagora.

Age: "Laramian" Structural type. The skam system occurs near contacts by

diffiJsion/infiltration metasomatÎsm (proxima! skams at Oravita and Baita Bihorului) and hundreds of meters from the contact by infiltration metasomatÎsm (distal skams at Ciclova and Baita BihoruJui).

Depositional environment. Contacts and roof pendants of pluton and thermal aureoles of pluton and apical zones of stock that intrude carbonate rocks and carbonate siliciclastic sequences.

Major tectonic setting. Andean-type or island arc subduction-related magmatism. Large scale zonality/associated deposit types. Contact aureole around the pluton

Mo-W skarn -- Bi-W-Cu skarn -- -- B marble. "Pentametallic" veins, U-Cu polygenetic, Pb-Zn replacement.

DEPOSIT DESCRIPTION Mineralogy. Scheelite + molybdenite + chalcopyrite + bismuthinite + Bi minerals

± sphalerite, galena, arsenopyrite, lollingite, glaucodote, gold, bornite, tetrahedrite, cubanite. Fluoborite, ludwigite, szaybellite and kotoite may be present.

Alteration. Dolomitic environment:' grossularite + vesuvÎanite inner zones; diopside ± phlogopite center~ clinohumite + chondrodite ± phlogopite outer zone; calciphyre, kotoite marble and brucite marble peripheral zones. Retrograde a1teration to talc, serpentine, chlorite, tremolite. In places high temperature fassaite, forsterite, spin el.

Ca1careous and calcareous-siliciclastic environment: ribbon rock of wollastonite and grossularite + vesuvianite alterning Jayers, metasomatised (skamified) hornfels is diopside + wollastonite + grandite. Retrograde alteration to epidote, actinolite, chlorite.

The pluton may be altered to periskam and grossularite + vesuvianite endoskarn. 19neous rocks found as dikes throughout the contact aureole are into

grossularite + vesuvianite skarn. Ore controls. Tabular Mo-W and pipe-like (Cu-Bi-W; Pb-Zn) ore bodies in

magnesianskams. Mo-W impregnations, pods and veins in ribbon rock. Associated igneous rocks occurring as dikes may be mineralized (Mo ± W stockwork in grossularite ± vesuvianite skarn).

Weathering. In places enrichment zone with secondary Cu-sulfides, native copper ~nd cuprite

Geochemical signature. W, Mo, Zn, Cu, Bi, Au, Ag, B Deposits: Băiţa Bihorului, Oraviţa, eielova.

39

40

Late Tertiary westward subduction during Neogene times (sensu Rădulescu and Săndulescu, 1973) gave rise to volcanics type and their deep-seated corresporldents, that rythmically from to Lower time, very eXJ:lressed in East Carpathians (Oaş-Gutâi region, Călimani-Gurghiu-Harghita volcanie ehain and Toroiaga-Bârgău-Ţibleş subvoleanie zone) and in the South Apuseni Mts (Metaliferi Mountains).

Ore deposits related to voleanics were considered during years as epitherrnaltsensu strieto) mineralizations (Au-Ag-Te eharacter prevailing in the South Apuseni Mts and Au-Ag and baSe-metal Oaş-Gutâi region) formed several in Badenian-Pontian times. Genetica} models based on Neogene magmatism evolution and related metallogenesis and significance of geological-geophysical evidence were provided by the South Apuseni Mts and Baia Mare geotectonie settings (Ghiţulescu, 1935; Ghiţuleseu, Borcoş, 1968; Borcoş, Andrei, 1984 ; Borcoş et 1994 a,b, 1997) and point to the intÎmate between seated intrusions and associated subvolcanic characters which, in turn, represent the infrastructure superficial/surf ace volcanic piles. .

More than 50 % of total resources estimates of Romania is given Neogene metallogenesis ot breccia pipe, veins and porphyry type found in two major units, the Carpathians volcanic arc and the South Apuseni Mts volcanics. The most important metals related to this event are gold, copper, lead and zinc.

The petrogenetic and metallogenetic characteristics of these Tertiary volcanic rocks have· been described by numerous authors, beginning in the century. Comprehensive reference works of more rece~t decades include those by Ghiţulescu, Socolescu (1941), Giuşcă et al. (1968 a,b, 1973), Rădulescu et al. (1973, 1981), lanovici et al. (1969, 1976), Ianovici, Borcoş (1983), Borcoş (1976, 1994 1997), ei al. (1973), Seghedi et al. (1994), Udubaşa (1970), Udubaşa et al. (1984).

20 - Loeation of porphyry and epithennal accumulations in the schematic structural metallogenetic map of the Metaliferi Mts. (ace. to et 1998).

n.:....!dll~~!.!!!!:>...!!.!m!.i!.!l!!!W.la.!.L.!::Y!lli!!!ill.!!~!.!.!!!J:;!!.!...!lL!:!!!<...Elll:!..ill..!:lll~ill..Jl!.!H! .. 1 - Bucium 2 - Groşi Nappe; 2 Valea Mică-Gâlda Nappe;

1 - Căpâlnaş-Techereu Nappe; 2 - Curechiu-Stănija 3 - Căbeşti 4 - Bejan Unit; 5 - Hospea Unit; 6 - Colţii Trascăului Nappe; 7 - Bedeleu Nappe; 8

Rameţi Beds - Mesocretaceous-post-tectonic cover; 1 Bihor Autochthon; 2 Codru Nappes system; 3 - Biharia Nappes system; 4 - Gosău Formation - post-tectonic ~=~"'-"-~~~~~!.!.!.!..!:~~~.!!.! 1 - Rapolt Crystalline; 2 - Bozeş Nappe; !::.:.....!Yrngm]~..lQ~: Jurassic (ophiolites s.I.); 2 - Eocretaceous (granite-granodiorites); 3 - Upper Cretaceous- Paleocene (banatites); 4 - Neogene (mostly andesitic associations); 5 - Pliocene-Quaternary (basalts); G. Conventional signs: I - Mureş fault (South Transylvanian Fau!t); 2 - fractures system geologically determined; 3 - fractures system geophysically deduced; 4 - Laramian nappes; 5 - Pre-Gosău Nappes; 6 - Meso-Cretaceous 7 -

8 - porphyry copper aceumulations; 9 - epithennal accumulation; Eocretaceous a) tholeiitic, b) 2 - Upper Cretaceous-Paleocene magmatites;.3 -Neogene magmatites. ~~.mL!!m~~lli.Y~~illl!!AtiQ!1§: 1. Baia de Arieş; 2. Roşia Poieni; 3. Roşia Montană; 4. Rodu-Frasin; 5. Conţu; 6. Corabia; 7. Tarniţa; 8.Trâmpoiele; 9. Haneş-Larga; 10. Stănija; 11. Muncăceasca Vest; 12. Mllgura; 13. V. Tisei; 14. Rovina; 15. Colnic; 16. V. Morii; 17. Musariu; 18. Vălişoara; 19. Bălta; 20. Câinel-Draica; 21. Voia; 22. Bolcana; 23. Hondol; 24. 25. Deva; 26. 27.Talagiu-Bratosin.

<

[TI ' lJ

N

41

42

Neogene volcanicity/metallogenesis in the South Mountains (Metaliferi Mts)

The volcanic activity of this unit evblved to the Pontian within intramontane bas ins which began activity in the NW -SE trending fractures Larami$1 system During the Neogene segments of this fracture system were U"'vU~'''''.1 determined a new involvement of the in new subsidence movements, thickening of deposits with the formation of numerous edifices subvolcanic structures and metaHogenic processes. The intersection points of the major tectono-magmatic (pre-Laramian) alignments, trending and NE-SW, alignments, constitute zones of volcanic and metallogenetic mobility Borcoş, 1 1976; Borcoş, Andrei, 1984). A general image stresses otit that within the same post-tectonic first developed a Paleocene mostly extrusive volcanism with altemations of ""' .... , ..... ..,. rhyolites included within a volcano-sedimentary formation et al., 1986). Mureş Valley, basalts, basanites are ta be found, which correspond to products formed at the expense (Rădulescu et rangmg between 38 and 46 m.y. (Krautner, 1985). to the of the Neogene volcanism Upper Pliocene-quaternary basait occur locally, i.e. two Detunata peaks in eastern vicinity of Bucium-Roşia Montana volcanic zone westernmost part of the Mureş at Lucareţ. are considered as intraplate magmatic

The volcanism extended northwards and an the border of the Bihor massif, but especially towards the west Zarand basin, prolonging towards the Pannonian Depression, a in which most the volcanic are burried in Neogene molasse (Ianovici et al., 1969). of volcanic activity generally proved by radiometric data 1981; Roşu et 1998) ta the was marked by sequences that can be grouped oel)en,oulg tectonic the petrochemical character, the age of products and the pre:sellce metallogenetic processes. The most important volcanic activity took place the Badenian, and Pannonian (Borcoş, 1976), the generated extrusÎve and intrusive products preceded by volcano-sedimentary formations that provide regional correlation ..... "' .. I.ro .. '"

It that at the Badenian metallogenetic processes took place, most quantitatively qualitatively ones being the andesitic (Ghiţulescu, 1941; Borcoş, 1976).

metallogenetic of Badenian locally and it is assocÎated with rhyodacites and andesites. mineralizations to the epithermal, mainly of auriferous type, without tendencies of primary variation, the composition of native gold, gold-silver sulphosalts and only subordinately of gold-base by hydrothermal products (adularization -silicification - argillisation). The this phase belong to two districts, Roşia Montană - Conţu and

! 1

43

The second Sarmatian( metallogenetic phase of the greatest importance is associated with the andesitic, dioritic arid quartz-dioritic subvolcanic structures. At present it is considered that the essential element in the evolution of the magmatic processes and in the position of the mineralizations is represented by the Neogene plutons lying at depths ranging between ± O and - 1,500 m; taking into consideration these depths as well as the geotectonic peculiarities specific to each zone, the succession of the vents with the location of the centres of maximum volcanic activity and metallogenic intensity can be established. In such cases the existing geological and geophysical data make possible the drawing out of a pattern of geological evolution and formation of the metalliferous (porphyry and hydrothermal) accumulations that may be applied to aH the Neogene vo1canic zones in the Apuseni Mts. A genetic model in the Zlatna district can be Igeneralized in aH the Apuseni Mts Subprovince, that is most of the deposits can be related to the subvolcanic bodies situated on the protuberances of the plutons vertically representing the transition to the volcanic structures and edifices, formed as a rule within the same phases of activity. Thus, special conditions appeared (large zones with high values of the geothermal gradients and great tectonic permeability) in which the metaHogenetic processes led to the accumulation of the metalliferous concentrations of porphyry ± hydrothermal type in the interval of some columns up to 1,500 - 2,000 high. The porphyry copper systems display the tendencies of primary variation of the mineralizations. In general, the gold and gold-silver base metal hydrothermal systems cross the zones with copper disseminated mineralizations; the superposition of the' hydrothermal transformation products specific to the two types of mineralization is also quite obvious. Locally there occur also tendencies of horizontal variation of the mineralizations, with transitions from the cupriferous to the auriferous base-metal mineralizations and even to the cinnabar ones (Zlatna volcanic zone). Such relationships enable the location of the accumulations with respect to the erosion level, the position of the accumulations differing from one zone to another and even within the same zone. There are cases in which the upper part of the porphyry copper type deposits has entirely been eroded along with the whole supposed succession of associated hydrothermal accumulations (Roşia Poieni); in some other cases the apical part of the porphyry copper structures reaches the surface level or undercrops (50-100 m), the structures being thus crossed or bordered by ba se-metal and gold vein systems (Valea Morii, Tarniţa, Bolcana); sometimes, the porphyry structures lie at depths ranging between 400 and 800 m (Musariu, West Muncăceasca, Tălagiu, Voia). The latter case provides representative examples in which the zonality of the mineralization and the supposed genetic relationship existing between the porphyry and hydrothermal type accumulations can be followed (Borcoş et aL, 1978; Udubaşa et al., 1981; Borcoş et al., 1983, 1994; Vlad, Borcoş, 1996). The cogenetic relationships between the two porphyry and epithermal mineralisation types formed in distinct sequences, but within the same process (phase), are also pointed out by the results of the sulphur isotopic study (Borcoş et al., 1982; Borcoş, Gaftoi, 1985).

The hydrothermal accumulations belonging to this Sarmatian phase show on the whole a prevailingly gold-silver character. They include native gold, gold tellurides and gold base-metal sulphosalts, gold base-metal sulphides in various parageneses and metallic mineral associations indicating a mineralogical succession in four geochemically distinct phases, often delimited also by tectonic discontinuities (superposed systems of mineralized fissures, brecciations) (Borcoş, 1976; lanovici et al., 1969, 1976). Depending on the local

44

conditions, the metaHogenic succession totally or partially, some showing a gre ater development or lacking Vertically, deposits show intervals

with of formed, constituting as a rule the the deposits . within the same or in different ore bodies, occur

various copper or auriferous-pyrite ore 1960 attention paid to in which the

auriferous base-metal mineralizations with significant contents (2-5 have intensely turned to account, especially native gold is stiH being identified. metallic mineral

association for this interval is formed mainly of pyrite chalcopyrite, mispickel deposition that generalized 70 % of the that vary quantitatively; the enrichments in chalcopyrite are known more Towards the final base-metal sequence and beginning gold an association of tellurides

sylvanite, pagyagite, hessite, oecurs only some deposits especially in Săeărâmb, Faţa Băii, present also subordinately in Stănija, Baia de ore deposits, or with tetrahedrite; in other deposits there occurs an assoclatlOn sulphosalts. associate such ores Bucîum-

deposit (Ianovici et 1969, 1976). Due to exploration works which have been carried out' (galleries, drillings) it could

established that in the lower part of thedeposits hydrothermal accumulations \,AJ""''''. prevailingly pyrite 15 mass of the ore bodies) pyrrhotite, chalcopyrite; sphalerite galena are subordinately omnipresent; hematite oecurs only locally, sporadically also arsenopyrite and marcasite.

Although copper dissemination mineralizations were a long time during exploitation (Deva, Valea Coranda, Trâmpoiele) and exploration works (Roşia Poieni, Musariu-Barza, Muncăceasca-Zlatna), the identification of the corresponding type as well as of the economic were mueh Iater -(Ianovici et al., 1969, 1 1977; Ionescu, 1974; Andrei, 1974; Calotă, 1974; Borcoş et al, 1 1976,1977,1978, 1983, 1989, 1994, 1998; Berbeleac et aL, 1976, 1 1981,1982, 1989, 1995; Vlad, 1983; Boştinescu, 1980, 1983, 1984).

The Deva deposit is mined out; the Roşia Poieni deposits are now being exploited; accurnulations at Tarniţa, Boicana Rovina are for exploitation; other accurnulations (Trâmpoiele, Haneş-Larga, Muncăceasca, Musariu, Voia, Talagiu as the most important ones) are only partly explored. The most favourable forming conditions of

mineralizations are due to (andesitic-dioritic) sequences the major structures and/or volcanic which are usually located at the of ophiolitic and Tertiary tectonomagmatic lineaments EW, NE and NW, respectively. The apical these mineralized bodies is frequently loeated in Sarmatian andesitie extrusive at depth come into contact with and/or metamorphic formations (most of thesituations) or even with metamoprhic formations (locally at Roşia Poieni).

character of copper is weB in most the succession and distribution the products two zones - a central potassic and a

marginal argillic ore ~ can distinguished; a few cases a phyllic zone also noticed (Borcoş et aL, 1978, 1983; Boştinescu, 1984). values and spatial distribution of the copper contents are nearly directly relatedto the potassic alteration; therefore one can

delimit relatively quasi-concentric zones with contents varying between 0.3 0.6 % in the central potassic halo; which can be locally characterized by higher gold>

values, of 0.7 and more. pre:sellce of in the copper mineralization is constant; a positive correlation

.... ",r',.,,,,,,>,,., copper and gold canbe established; global Cu/Au ratio varies from one district to another (Borcoş et al., 1983). the Deva and Roşia Poieni deposits, where the basement is predominant1y crystalline, one can notice a concentration towards the

depth of the molybdenite - 30-1 ppm compared to a decrease the I'n ... ' .... ""r

and gold contents. Molybdenite with lower values 40-90 ppm (Boştinescu, unpub1. data).

Conceptual ore forming models. In terms of tectono-magmatic features, porphyry-epithermal relation, composition and intensity of mineralization and alteration following models have been identified (Vlad, 1996; Borcoş, Vlad, 1997):

- two of copper that is Valea Morii porphyry epithermal model Roşia Poieni porphyry with pyrite halo model;

- the non-porphyry environment is also represented by two models, Roşia

Montană composite system of brecCia pipe and S~cărâmb vein set. main characteristics are presented in Tables 6, 8, 9 and Figures 21,

)(

:0

x

x

x x

x + + ... ...

)( ~//+ + + ... ' + ® ., /' + + + + ... ... + /' ... + ++ + I I I

-1- -1- -1-

2km

x

:0

x x

-1 x .1 .... \ )( / +

-'-J

-2

/'+ /'+

+ + + ... +

+ + + + + ... + + ... +

... + + ... +

-:- ®

Fig. 21 - Tertiary porphyrymodels in the South Apuseni Mts (ace. to Vlad, 1996). Key: A. Model Valea Morii; B. Model Poieni: 1 - syn-ore palaeosurface; 2 - level of erosion; 3 -siliciclastic rocks of the 4 - Mesozoic rocks; 5 - ophiolites; 6 - porphyry copper

7 - composite subvolcanicstructure; 8 culmination of pluton; 9 - pluton; 10 - fracture; 11 - Au-Ag and Au-Ag-Pb-Zn sets ofveins. .

',i.

46

TABLE 6 - Model Valea Morii-Diorite Type, Cu-Au Polyascendent Evolution Epithermal Veius Halo (M IX in Fig. 21A, Plate 1)

DESCRIPTlON. Stockwork veinlets of chalcopyrite ± magnetite. bomite in porphyritic intrusions of subvolcanic type volcanic rocks.

GEOLOGICAL ENV1RONMENT Rock types. Quartz andesite to quartz diorite and andesite flows. Age: Structural type. porphyry copper system is centered on subvolcanic apophyses

corresponding to culminations of deep-seated plutons. Depositional environment. Volcano-plutonic complexes at the intersection

of the main ophiolitic, Laramian and T ertiary tectono-magmatic lineaments trending E-W, NE-SW and NW -SE, respectively. The apical part of the mineralized system is commonly located within T ertiary volcanic rocks, sandstones, conglomerates and pyroclastics. depth igneous rocks come in contact with Mesozoic sedimentary and ophiolitic rocks and pre-Mesozoic metamorphic rocks. The T ertiary igneous assemblages occur in molasse

controUed by reactivat ion of early fracture systems. Major tectonic setting. Back arc reactivization along extensional fault systems. Large scale zonality- associated deposit types. Cu-Au stockwork in hydrothermally

altered subvolcanic body -- Au-Ag ± Te and Pb-Zn ± Cu veins in hydrothermally altered volcanic rocks -. pyrite halo some intruded rock.s Mesozoic ophiolites).

DEPOSIT DESCRlPTION Mineralogy. Chalcopyrite ± magnetite with ilmenite Of rutile inclusions + pyrite

with rutile inclusions ± bomite, sphalerite, tetrahedrite, galena, goJd, molybdenite veinlets and chalcopyrite + magnetite + pyrite impregnations potassic zone.

AJteration. Potassic alteration (K feldspar + biotite with superposed anhydrite, adularia, albite, chlorite, actinolite, calcite) in subvolcanic bodies. Peripheral earIy and propylitic alteration (chlorite + actinolite + epidote + calcite).

The alteratÎon pattern is similar to the diorite type .. Ore controls. Veinlets and fractures of quartz; chlorite, epidote and sulphide are

closely spaced. Weathering. Bleached country rock, "limonitization" Geochemical signture: Au, Ti, Mn, Pb, Zn, Ag, Mo, Sb, Bi, Ni Deposits I Prospecţs: Valea Morii, Musariu, Bolcana, Voia, Colnic, Tălagiu,

Haneş-Larga, Trampoiele, Muncăceasca W, Valea Tisei, Tarniţa.

TABLE 7 - Model Roşia-Poieni-Diorite Type, Cu-Mo Polyascendent Evolution Pyrite Halo (M VIn in 21 B, Plate 1)

DESCRIPTION. Chalcopyrite + pyrite hydrothermally altered porphyritic intrusÎon.

GEOLOGICAL ENVIRONMENT

molybdenite In stockwork In

Rock types. Quartz andesite to quartz diorite porphyry stocks and related breccia intruding crystaHine basement, Cretaceous and T ertiary sedimentary rocks.

Sarmatian. Structural type. High-Ievel intrusive porphyry contemporaneous with faults

breccia pipes. . Depositional environment. Plutonîc cupola and related subvolcanic intrusion

tectonic alignments striking or NW-SE in the Tertiary molasse basin. 19neous assemblage penetrated in the crystaUine pre-Mesozoic basement and flysch and Badenian-Sarmatian molasse.

Major tectonic setting. Back arc reactivization along extensional fault systems. Large scale zonruity associated deposit types. Not expressed. DEPOSIT DESCRIPTION Mineralogy. Pyrite + chaicopyrite + molybdenite ± magnetite, hematite veînlets

with subordinate pyrrhotite, bornite, sphalerite, galena, digenite, enargite-famatinite, lusonite-stibiolusonite, tetrahedrite-tennantite in potassic zone.

AJteration. Potassic alteration (biotite + quartz ± Q-feldspar and anhydrite) in the porphyritic intrusion, partly replaced by albite ± actinolite. Argillic alteration (kaolinite + illite + montmorillonÎte ± alunite) at the margin of the subvolcanic body. Early propylitization (calcite + chlorite + rutile + albite) in surrounding volcanic The alteration pattern Îs similar to diorite type.

Weathering. Restricted chalcocite blanket and .... v'.,"' ...... Geochemical signature. Cu, Mo, Mn, Au, Pb, Zn, As, Bi, Se, Ta. Deposits Prospects: Roşia Poieni, Bucureşci-Rovina, Deva, Măgura,

47

48

TABLE 8 - Model Roşia Montană-Precious Metal Breccia Pipe and Veins , (M X in Fig. 22A, Plate 1) .

DESCRIPTION, Epithermal gold in volcanic rocks and associated sedimentary rocks.

GEOLOGICAL ENVIRONMENT. Rock type. Dacite to rhyodacite and quartz andesite and associated volcano­

sedimentary andsedimentary siliciclastic rocks. · Age. Badenian Structural type. Fracture and breccia minentlization in dacite flow above

subvolcanic plugs . Depositional environment. Volcano-plutonic complexes situated at the inters~ion

of the main ophiolitic, Laramian and T ertiary tectonomagmatic alignments in molasse basins. The regional lineation is NW -SE and . exhibits local phreatomagmatic explosions with associated ore formation. Breccia pipes as apex of the mÎneralized system occur in the volcanic edifices or toward their margins. At depth the igneous rocks comein contact with Mesozoic siliciclastic and ophiolitic rocks and pre-Mesozoic crystalline schists. .

Major tectonic setting. Back arc reactivization along extensional fracture systems. Large scale zonality - associated deposit types. Epithermal gold (quartz-adularia),

polymetallic veins and replacement. DEPOSIT DESCRIPTION Mineralogy. Pyrite + arsenopyrite + gold, subordinate sphalerite, chalcopyrite,

galena, alabandite, tetrahedrite. Peculiar proustite, pearceite, polybasite, argentite. A1teration. Regional propylitization, quartz + sericite + adularia, argillic alteration. Ore controls. lntimate association of quartz-adularia alteration with gold shoots. Weathering. Bleached country rock, "limonitization" Geochemical signature: Au, Ag, As, Sb, Bi, Ti, Se, TI. Deposits: Roşia Montană, Radu-Frasin, Cainel, Draica, partly Baia de Arieş.

TABLE 9 - Model Săcărâmb-Precious Metal Veins (M in Fig. 22B, Plate 1)

DESCR1PTION. Epithermal Au-Ag-Te. siliciclastic sequences, local polymetallic veins.

GEOLOGICAL ENVIRONMENT

volcanic rocks and associated

Rock types. Quartz andesÎte and andesite and associated siliciclastic sedimentary and volcano-sedimentary rocks.

Age. Sannatian. Structural type. Vein and stockwork sets in apical part of subvolcanic plugs. Depositional environment. Volcano-plutonic complexes situated at the intersection

of the main ophiolitic, Laramian and T ertiary tectonomagmatic alignments in molasse basins. The apex of the mineralized system is common1y located within T ertiary volcanic and subvolcanic rocks and siliciclastic rocks. The basement consists of Mesozoic siliciclastic rocks and ophiolites.

Major tectonic Back arc reactivization along fracture systems. Large scale zonaJity - associated deposit types. Polymetallic veins or stockworks

and replacement, distal gold metasomatic disseminated. DEPOSIT DESCRIPTION Mineralogy. Stage 1 is pyrite + pyrrhotite + arsenopyrite + sphaJerite + galena +

chalcopyrite + alabandite. Stage 2 is represented by common sufphides and nagyagite, krennerite, silvanite, altaite, hessite, petzite, teUurium, tetrahedrite, boulangerite, jamesonite, antimonite, arsen, gold quartz + carbonate (mainly rhodocrosite ) + clay mineraJs gangue. '

A1teration. Regional propylitization; chloritization, quartz + adulana, sericitization, argillic alteration.

Ore controls. Tentency of horizontal and vertical zonaJity. Quartz + adularia alteration is intimately associated with Te-Au-Ag mineralization, sericite and argillic alteration i5 associated with Pb-Zn-Au-Ag mineralization and chloritization with pyrite­Pb-Zn mineralization.

Weathering. Bleached country rock, "limonitization" Deposits: Săcăramb, Stănija, Baii, partly Baia de Arieş.

49

50

5 ~J8) /.. .. ~"-"

'\. _,­I

-0.5

22 - Tertiary models in the South Apuseni Mts. to Borcoş, Vlad, 1997). Key: A. Model Roşia Montană; B. Model Săcărâmb: I - syn-ore palaeosurface; 2 - level of 3 -siliciclastic rocks ofthe Tertiary molasse: 4 volcanic products; 5 subvolcanic body; 6 - rocks (a-Mesozoic ophiolitic and associated sedimentary rocks; b - crystalline schists and Mesozoic sedimentary rocks); 7- phreatomagmatic explosion breccia; 8 - culmination of pluton; 9 - plutons; 10 - breccia pipe; 11 - vein; 12 -stockwork mineralization.

At Baia of breccia pipe was identified by Ghiţulescu in 1958 (unpublished data). This was by the percussive blast of some punctiform volcanic eruptions, with volcanic ash without lavas or other form of liquid magma. In most of the cases, breccia pipe usually with pipe-like formes represents ideal structural tn.ips richest concentrations ( Ghiţulescu, Pitulea, Ghiţulescu, 1979) ( Figs. 24).

23 - Schematic section through andesitic body to Ghiţulescu, 1983, with completions)

1, 2, 3 - successive andesitic intrusions; 4 culmination; 5 ~ 6 -crystalline 7 - breccia 8 - gold stockworks; 9 gold veins; 10 - fractures.

800

500

.t.O

-500

-1000

-1500

1....-_-'

NV

II

II

v

II

II

II

II

II

II

II

II

v

v II

II

II

+

+

1

II

+

+

+ +

II

v

+

+ + + + + + + +

2 3 1....---'

51

SE Prunilor V.

Ambru

II

II

II

II

II

II II v II v II II

II II II II II II

II

II II

II II II II II

II II II

II II II

II II

+

4 5 6

52

m 900

700

600

SIlO

400

300

200

100

-100

-200

-300

-400

-500

1 f9v~

V

V

II

II

V

V

V ,

I I I VV""(+) I

I , , I

I.IJ I

v\ , \ a. \

I , I , I , , I

V \ a. I , I I

VV'f4 I I I I I « , , I

VI t;,:::s. I I

U ,-I ,-

!VV~u , ,

I • I I.IJ I I ,

/ I

II I I

I I I I { i'l +

T'_".. .. _ ... '++ J ~....... "--... I I <' .... _"" "-7+ -----_#

v

v

""

""

~

....

=:::

Z

Z

24 - representation of the Afiniş breccia (acc. to Ghiţulescu et aL, 1979). - pipe-like polygenous brecciform formation

with of macroporphyry andesite and crystalline schists; 2 - pipe-like breccîform formation with two andesite types (macro- and microporphyry); 3 - pipe-like polygenous breccîform formation with microporphyry andesite and crystalline schists; 4 - brecciated microporphyry 5 -apex of diffused mineralized microporhyry subvolcanic body; 6 - Afiniş 7 -crystalline 8 - drilling; 9 - level.

The mineralising solutions penetrated the andesite blocks, already affected by hydrothel11lal alteration, an impregnation of metalliferous sulphides.

developed as a metasomatosis, whose intensity decreased from periphery to the core the block, so that, in certain cases, it became sterile. richest mineralisation was formed by the deposition of and metalliferous minerals in empty space. composltlOn this mineralisatioin is relatively including approximately 6% pyrite, 3% arsenopyrite, 1% 0.2% hematite 0.1 % 0.05% alabandine, 0.05% chalcopyrite, 0.01% galena and 0.01% gold and silver stibio-teUuride (Sb

(Niţulescu et aL, 1957).

53

The most product of this type of mineralisation is by a deposit of microcrystalline intergrown with crystals of pyrite,

gold bearing arsenopyrite. As crystallisation forms it is worth mentioning filiform omated by crystals of gold bearing The mineralisation occurs

as compact siliceous crusts a dark grey colour (black crusts covering the andesite blocks). empty space between blocks is filled, more or completely, by short and

of white quartz in association with small crystals sulphides. carbonates (calcite, rhodochrosite) and in the .............. ..

is theprevailing exceeding is' better (up to 90%), it is rieh in quantitative relationship between gold, arsenic and silica is

Uil..," ...... ''', 1983).

Neogene volcanicity/metallogenesis in the Oa~-Gutâi Mountains

The Oaş-Gutâi volcanic area represÎ'!nts·~ distinct sector of the , '

proceeding almost continuously from the West . to the East were formed in the same geotectonic .., ... ~,,, .. ~.,' volcanic and metallogenetic evolution (Fig. 25). towards the Transcarpathian ' their igneous built :tip the southem portion of

Viskovo-Beregovo whereas the Pannonian-Pliocerte volcanic suites with base-metal and mineralization. In the Gutâi Mts the volcanicity acted

and almost from Badenian to . giving to numerous metaUogertetic sequences of base-metal and Au-Ag "h~'1"';I('tp1"

significant economic (Borcoş et al., 1973; et al.~ 1973; Borcoş et 1996; Lang, 1979).

The recent geotectonic setting infered from geological-gşophysical data in Oaş-Gutâi region an composed plu,tons in genetical relations

with several fracture that controlled developmentlemplacement of the '-"'J"'·V''''.'',",U. 1964, 1965; et aţ.,1994,Borcoş et 1973,

The pre-Neogene consists of metamorphic rocks and Cretaceous ... Paleogene sedimentary rocks, a pre-Neogene latitudinal

system. The major ruptural line - Drago'ş Vodă fault,)s situated on the southem A' of the Gutâi Mts and extends, significantly; strike (1 OO~ toward up to

Carhbaba and 120 km toward West beyond pluton as weU as the pluton d.eli~eated in the O~ ,area occur in an uplifted compartment of the twsement. It is likely that simIlar fractures strlkmg are to be found north Vodă fault with extenS:lon

the Oaş region and to adjacent volcanic Hungary and anomalies deep-seated plutons, too. Additionalregional sets

especially (Borcoş et aL, 1980). cut the plutons promoting tectonic mainly of levogyre displacement. Such reactivation acted

.V"' ..... 'lU)' during the plutonic/volcanic events, fracturation with important metallogenetic distri\:mtion (Borcoş et al., 1996).

54

'" .. ~\ \~ ~ :~: ~D'" ~-: D~· ~ .:' ~ < < " r-< . ', m

Q

m

::J o; '" " el

O I I ...

;;:; , I I

- i5

: '; ', {\ '::::': . ~ .. ' \..1

Z o J>

Altemation of sedimentary with igneous sequences and ......... v •• ..., delineate three successive volcanic phases during ... " .......... j'u ... u~. llQiCeIle ,""P"/V''''

(Borcoş et al., 1973, 1994, 1996). event is Badenian-Sarmatian and exhibits a

rhyodacite); ignimbrite and volcano-sedimentary ror:manOllS lOc:ate:a on south-eastem part of the Gutâi Mts and ..... ","""~.rt in the Transcarpatian region and in the southem Hungary

The second event is mainly andesitic and polystadial. the igneous products are widespread in both

55

three ore forming sequences related to Sarmatian Pannol1Îan (.U""'''''''J'~''''' and Pontian andesites. The most representative occurrences are found in

part of the Gutâi Mts and aH over the Oaş Mts. The third event started at the end of Pontian in the Pliocene.

The character is mainly andesitic, with frequent extrusive .... ~~~ .. found in the northern

occurrences found in the Transcarpathian chain.

In the Oaş-Gutâi region, numerous undertaken, yielding significant data concerning the structure, umeOllS activities. The Neogene pluton of the Gutâi area, especially contact ""'Al''''''''',,",hll;:tn in surrounding rocks and its homogen~ous quartz-dioritic emplacement preceded or acted simultaneously with the early Sarmatian of this kind is going to be provided by investigation ruptural and radiometric behaviour displayed by a co-operation team and "Cuarţ" S.A. Baia Mare.

Ore deposition is related to corresponding to ore forming events 1972, 1973). These districts southern border of the Gutâi massif, activity.

1-''''''''''''''''' with metallogenetic character et al., 1974 a, 1 1976, 1994, 1996; Stanciu,

a continuous metallogenetic zone along foHowing the eastward migration of the volcanic

Early metallogenetic base-metal and gold mineralization, confined to Sarmatian pyroxene andesites the Ilba-Nistru district. It delineates two NW-SE metallogenetic alignments. The 'is a tectono-volcanic sensu structure; vein sets are commonly normal on Îts axis. southem lineament Îs a fracture ------------------------.-------------------------------------------------------------------------------------

Fig. 25 - volcanics in the Alpinestructural setting ofthe Oaş-Gutâi region to et al., 1994).

Key: 1 - Neogene molasse; 2 - Post-ore Upper Pontian-Pliocene andesites; 3, Sarmatian-Pontian andesites (metallogenic phase); 4 - Badenian volcano-sedimentary formations; 5 - Paleogene flysch; 6 - metamorphic formations; 7 - fault; 8 - nappe; 9 x tectonic 10 x- Neogene pluton; II x - pluton culminations; 12 x - Dragoş Vodă transcrustal 13 x fractures partly reactivated; 14 x -fractures partly 15 main 16 - mining fieJds (1. Racşa, 2. I1ba, 3. Nistru, 4. Săsar, 5. Valea 7. 9. Valea Negrii, 10. Dealul Crucii, II. 12. Baia Sprie-Şuior, 13. 16. Băiuţ, 17. Văratec, 18. North Băiuţ, 19. Jereapăn)

x Geophysical elements

56

sensu stricto with metallogenetic role; it contains breccia and impregnatioins bodies of local Cu l' .... ~' .. ~Il'·Tp ..

The subsequent metaUogenetic phase is of prevailing Au-Ag character and was formed in relation to Pannonian quartz andesites. The ore occurrences are distributed in the central part the portion of the that is the Săsar-Valea Roşie district. The most important alignment is found the South, in connection with a sector of the important Dragoş Vodă fault. The Săsar and Valea Roşie deposits represent vein groups with numerous branches usually disposed normal to the axes of the lineament.

The metallogenetic phase is association with Pontian pyroxene andesites, / found especially in the central-eastern part of the massif. This phase is more complex,

showing an goldJbase-metal even character, specific to almost alI deposits and with a remarkable vertical Major deposits are controlled by NE-SW fractures the signiticant Dragoş Vodă fault. The following metallogenetic fractures are recognized from

. west toward east: Dealul Crucii - Herja - Baia Sprie - Şuior - Băiuţ -Văratec and the tectono­vo1canic alignment with veins disposed normal to the axis. They show a polystadial formation, with specific recurrences of Au . and base-metal mineralization; complex breccia pipes with irfegular shape and large sizes are common. Along the same SW-

fracture system Crucii - Băiuţ - Văratec Au and base-metal deposits consist of ve in related to subvolcanic bodies. The Cavnic-Roata tectono-volcanic alignment comprises vein groups of similar polyascendant character, controlled by simultaneous ore forming and tectonic brecciation.

The above-mentioned districts coritain sequences. of metallic/gangue associations that can be used as geochemical markers or discriminative elements of those· three metallogenetic events.

According to recent results (Lang et 1994; Kovacs et al., 1998) the Gutâi Mts metallogenetic activity developed 'in two main phases: the tirst phase took place in the

Pannonian (11.5 - 10 m.y.), including metallogenetic events from Uba - Nistru and Săsar - Dl. Crucii districts, and the second one is in the Upper Pannonian (9.4 - 7.9 m.y.), including Helja - Băiuţ district. The metallogenetic activity in the Oaş and Ţibleş Mts is contemporaneous with the second phase ofthe Gutâi Mts (9.6 - 7.8 m.y.). presence of a gap (0.5 -1.5 m.y.) between the of the epithermal mineralisations (adularia-sericite type) and the host magmatic in this region is very similar as compared to other subduction-related occurrences wor1dwide.

~:W:::'E:Jl!..!:lli;~'.E..J!:!!J'.!!!.L%J::"!:!!;!!ill11!!~ ectono-l1na~~mc:ltic setting, alteration, zoning and . ore TrIl"""'''' correspond to two models, that is Baia Sprie breccia (phreato-magmatic explosion type) - ve in deposit with base-metals and precious metals, and Cavnic ve in deposit, with base-metal and (Vlad, Borcoş, 1997) (Tables 10, 11, Fig. 26).

Neogene metallogeny in the Toroiaga-Bârg'ău-Ţibleş subvolcanic zone

The so-called subvolcanic zone the Neogene volcanic chain of the East Carpathians contain base metal ores mostly of vein type, with subordinate disseminated and breccia-pipe ores. The host are andesitic composition (Toroiaga, Rodna, Bârgău) and

57

1klJl A 1.Skm B

!O

-1

--1

Fig. 26 - Tertiary epithennal models in the Oaş-Gutâi Mts. (ace. to Borcoş, Vlad, 1997). Key: A. Model Baia Sprie; B. · Model Cavnic: 1 - syn-ore palaeosurface; 2 - level of erosion; 3 - volcanic products; 4 - siliciclastic rocks of the Tertiary molasse; 5 - homf€1S in Paleogene sedimentary host rocks; 6 -subvolcanic body; 7 - phreato-magmatic explosion breccia; 8 - culmination of pluton; 9 - pluton; 10 - crystalline schists; 11 - vein; 12 - stockwork mineralization.

display a much more complex structure and composition in the Ţibleş Mts. Here intrusive rocks of monzodiorite and granodiorite composition form the central part of the massif. The peripheral zones consist of rocks of andesitic composition and form either a nearly continuous belt around the intrusive nucleus or small to very small bodies intruded into surrounding Paleogene sedimentary rocks. The metallogeny of the Ţibleş massif is also a very complex one, displaying a well-developed regional zoning, with high temperature associations (pyrrhotite, arsenopyrite, pyrite, iron-rich sphalerite etc.) in the central part, being nearly completely surrounded by a belt of. lower temperature associations (stibnite, kermesite, cinnabar, berthierite, owyheeite etc.) (Fig. 27). In addition, in the southern · part of the intrusive nucleus the veins are slightly enriched in copper, a fact which parallel both alteration types . (K-feldspar, biotite etc.) and mineral parageneses (veinlets of magnetite and chalcopyrite) suggesting the presence of a hidden porphyry copper system (Udubaşa et al., 1983, 1994; Pintea, 1998).

The Toroiaga veins contain Cu~Pb-Zn ores with local gold enrichment zones. In addition to the major common sulphides, numerous sulphosalts were described here, both Sb­dominated (Steclaci, 1968) and Bi-dominated ' (Cook, 1997) . . Generaf features of the petrography and geochemistry ofthe whole ore field are given by Borcoş (1967), Borcqş et al. (1982), Berza et al. (1981). .

58

The Rodna ore is related to subvolcanic rocks of andesitic composltlOn intruding metamorphic rocks that host stratiform Pb-Zn ores in carbonate rocks. The hydrothermal ores form both replacement,bodies in carbonate rocks and dissemination within

TABLE 10 - Model Baia Sprie-PolymetaUic and PreciousMetal Breccia Pipe and Veins (M VI Fig. 26A. Plate 1)

DESCRIPTION. Epithermal and polymetaHic veins and breccias. GEOLOGIC AL ENV1RONMENT Rock types. Quartz andesite and andesite and associated sedimentary rocks. The

igneous rocks belong to the Later T ertiary volcanic arc of the East Carpathians. Age. Sarmatian-Pannonian, Pontian Structural type. Epithermal system controlled by subjacent pluton situated in major

crustal fault. Depositional Volcano-plutonic complexes. Deposits related to

subvolcanic level undergoing phreatomagmatic explosion aIong reactivated NW-SE and SW-NE regional fracture sets. The Late Tertiary pluton of quartz. diorite composition Îs ·situated at 2 to 4 km depth. The metalliferous systems extend 1.5 km away from the apical part of the plutonic culmination.

Major tectonic setting. Island-arc volcanic setting. zonality/associated deposit types. Epithermal gold (quartz-adularia),

polymetallic veins. DEPOSIT DESCRIPTION Mineralogy. Early stage with pyrite + chalcopyrite + hematite, scheelite, magnetite,

wolframite in ch10rite + quartz + ankerite + barite gangue. Subsequent stage with pyrrhotite + sphalerite + chalcopyrite + galena.

Alteration. Regional propylitization, ch1oritization, quartz + adularia, sericitization, argillic alteration.

Ore controls. Tectonic: fractures and anastomosing fissural systems. Vertical zoning: top to bottom Au-Ag -- Pb-Zn-Au-Ag -- Cu-Pb-Zn -- Cu +- W. Selective

of gold with quartz-adularia alteration, polymetallic ores with argiHization and copper with ch1oritizat10n.

Weathering. Bleached country rock. "Limonitization". Geochemical signature. Cu, Pb, Zn, Au, Ag, As, Sb, Bi, Se, Cd, G3., Te, Ti, W,

Co, Ni. Deposits: Baia Sprie, Suior, partly Baiut-Varatic, VfTapului-Mihai~Nepomuc.

the breccia-pipes (as described by Socolescu et al., 1977). The ores contain iron-rich sphalerites, pyrrhotite, pyrite, as well as native gold' (mostly the

Ag and some sulphosalts (Udubaşa, 1970, 1 1984). Small ore occurrences exist also in the Bârgău Mts, forming either veins (Pb-Zn-As

and some gol9-, e.g. Colibiţa) impregnations in and Paleogene rocks. They are quite similar to the ore occurrences found in the southwards

situated Că1imani Mts (e.g. Stânceni) (Peltz et aL, 1981).'

TABLE 11 - Model CavnÎc-Base Metal and Precious Metal Veins (M VII in Fig. 26B, Plate 1)

DESCRIPTION. Epithemial gold and polymetallic veins. GEOLOGICAL ENVIRONMENT Rock Quartz andesite and andesite and associated sedimentary rocks. The

igneous rocks belong to the Late Tertiary volcanic arc ofthe East Carpatmans. Age. Sarmatian-Pannonian, Pontian Structural type. Epithermal system 'controlled by subjacent pluton situated in major

crustal fault. Depositional environment. Volcano-plutonic complexes. The mineralized system Îs

commonly located witmn volcanic rocks. It is centered on subvolcanic apophyses corresponding to culmination of the quartz diorite pluton. The mineralized column is 1 lan mgh. At depth the igneous rocks come in contact ~th Early T eftiary siliciclastic rocks converted into homfels. The sedimentary rocks are displaced along distensional N-S fractures.

Major tectonic setting. Istand-arc volcanic setting. Large scale zooality associated deposit types. Epithermal gold (quartz-adularia),

polymetallic vems. '

59

DEPOSIT DESCRIPTION Mineralogy. stage with + chalcopyrite + hematite + magnetite

quartz ± chlorite, epidote gangue. Stage 2 is pyrite + sphalerite + galena + chalcopyrite + arsenopyrite in quartz, adularia, carbonate, clay minerals and barite gangue. Stage 3 contains pyrite + galena + sphalerite + chalcopyrite + tetrahedrite in quartz and carbonate (especially rhodochrosite) gangue. Last stage with pyrite + tetrahedrite + boumonite + jamesonite + gold + realgar + orpigment in quartz, gypsum and carbonate gangue.

Alteration. propylitization; chloritization, quartz + adularia, sericitization, argillic alteration.

Ore controls. T ectonÎc: major fracture and related fault systems. A tendency of vertical zoning from Cu-Pb-Zn bottom zone to Pb-Zn-AlJ-Ag toward top.

Weathering. Bleached country rock, "limonitization" Geochemical signature. Pb, Zn, Cu, Au, Ag, Cd, Ga, In, Bi, Sb, Mn. Deposit!: Cavnic, Roata, Herja, Ilba, Nistru, Dealul Crucii.

The Toroiaga and Rodna ore fields were exploited many years (the Rodna mine is dated 1 , when a significant silver production was yielded) and the ore bodies are mostly exhausted. The Ţibleş area waS intensively explored. resulted ore reserves quite good quality are partly oxidized, a fact hampering further mining activity. However, the exploration of the southern part, showing features of a porphyry copper . largely unexplored.

o 1 Km

2 6

1.....2:--=!J 3 1 ..::..:.... 1 7 11 Cu

4 8 12 13

fig. 27 map oflhe Tibles Igneous Complex (ace, 10 Udubasa el al., 1984), Key: 1 - quartz monzodioritie rocks; 2 - dioriles granodiorites, quartz andesites, dacites, pyroxene and homblende andesites; 3 and dacites; 4 - pyroxene andesite, quartz and andesitoidic rocks; 5 - sedimentary roeks; 6 - contact aureole; 7 - veins and disseminations; 8 - copper enriched ores and the system; 9 - disseminations; inner zone of high temperarure vein assemblages; II -external beII of lower temperarure vein 12 - tourmaline occurrenc~s; 13 -ternary diagrams analytical data of the primary ores (larger triangles) and limonites (sma!\er triangles).

0'1 <O

Neogene volcanicity/metallogenesis in the Ciflimani-GuI'ghiu-Hal'ghita Mountains

61

The Călimani-Gurghiu-Harghita volcanic chain the largest occurrence area of Neogene volcanics not only in Romania but also in the whole Carpathiarts. It consists of a 160 km Iong continuous volcanic with decreasing width, height and volume from North to South. ..

chain displays a roughly median position the Carpathian structural units (Upper Cretaceous to Paleogene "Transcarpathian Flyschll unit in the north, the "Crystalline-Mesozoic zone" unit in the Cretaceous Flysch" unit 'in southeast) and the Neozoic Transylvanian Contrasting crusta) structure of two major

is by their crustal thickness as pointed out magnetotelluric investigations: about 40 km beneath the East Carpathians and about 30 km beneath the Transylvaruan Basin (Stănică et al., 1986, 1990). The volcanîc chain thus appears to be spatially to the structural boundaries between them, South Harghita segment that crosscuts the East Carpathian tectonic units.

tectonic of the Călimani-Gurghiu-Harghita chain based on complex geophysical suggest the major NW -SE trending tectono-magmatic alignments (controUed probably by collision and subduction geometry), strike-slip fractures (trending generally E-W) and distensionaI fractures (generally N-S trending) (Fig. 28). PostcoHisional compressive· tectonism was stiH in the outer Carpathians during volcanism in the Călimani, Gurghiu and North Harghita segments of the chain, while volcanic activity along the South Harghita chain, Le. the terminus segment, was coeval with

Pliocene to extensional tectonism. This resulted in intrarnountain formation in the nearby and in within- plate alkali basaItic volcanism. in the neighboring

Mts. (Rădulescu et aL, 1973, 1981; Seghedi et al., 1994;.Balintoni et aL, 1996). Increasing arnount of geological data that the volcanic structures """",,", .. ,.,. .. ,1">

to the Că1imani-Gurghiu-Harghlta chain consist of a central volcanic zone with subvolcanic intrusive . bodies in Îts infrastructure, an intermediate zone corresponding to volcanic cone (mainly consisting ,of lava flows) a mainly volcaniclastic zone. Explosive­

volcaruc activity prevailed in alI the stratovolcanic edifices building up a chain adjoining and partially overlapping composite with well-developed peripheral volcaniclastic aprons.

Typical calc-alkaline rocks ranging from basaltic (ţI1desites to dacites form the great bulk of chain (Rădulescu, 1973; Peltz et aL;' 1973),rSmall volume of tholeiitic volcanic products and high-alumina basalts in tile G~ Mts. along-chain short distance variation from' t)(pically calc:-alkaline to shosh"Ortit.1b-composition was pointed out in the southemmost segmertt (Seghedi et 1986, 1987)~- .. , .

The whole Călimani-Gurghiu-Harghita' chaÎn.rwas the site atypical along-arc migration the volcanism during Neogene and Quatemary times (Rădulescu et al., 1973,

et al., 1987). Volcanism began in the CăIimani Mts at 9.5 m.y. over an area already hosting subvolcanic intrusions (10.5 - 9.8 m.y.). Volcanism ceased at about 0.2 m.y. South Harghita at the end of a spectacular short-distance age progression along this chain terminus (Szakacs et unpubLdata).

62

,·~~~Z,-:,:

----------~{ :: Rrai~ · . -=--=.=:= -=. =-=. :==="';~: : "·:~ .~i.: ..

': ., '. 12 ... .'

.0 13 a b

• 14

• 15

• 16

" 17

'C) 18

a b

o 4 BKm '--' ........ .-... .....

>

;,i

LEGEND

1:-:-:1 11 ,1,',',1 2

1=-=<=1 3

1 14 It :\:-.>1>1 5

Q b c f\ 6

• • 7

.............. 8

++ 9 10

..... -. , a ~! +,1 " ' .. ,." , ,, ..... b ... _ 1

Fig. 28

63

28 - GeologicaJ sketch ofthe Călimani-Gurghiu-Harghita volcanic chain with structural and. metallogenetic features (ace. to et al., 1994).

Key: I - East Carpathian structural units (Crystalline-Mesozoic Zone and Zone); 2 - Flysch (Upper 3 - Basin molasse (Miocene); 4 -Intramountain depression Pliocene to 5 - Călimani-Gurghiu-Harghita voleanic chain: a) intrusions; b) voleaniclastic e) stratovoleanic edifiees (CL = FL Fâncel-Lăpuşna, ST = Seaca - Tătarea, S = Şumuleu, CF O Ostoroş, le Ivo-Coeoizaş, V = LL = Luei.»Lazu, C = Cucu, P CM = Ciomadul); 6 - Calderaş and craters (topographie !LJJ;;~!!!f...JillQ..jID!!~:&.ill1lJ.!J~~~Q!l...@QJl!J!Y§!~.Jli!!LUilim~t!2!!: 7 - Major teetono-magmatie alignments; 8 - Major strike-slipe faults; 9 - Major distensional fractures; 10 - other major fractures; Il • volcanism-related intrusions: a) outcropping; b) partially or totally inferred from geophysical data. ~~lt!!!J[.Qg!~~LLJj~~: 12 - outlines of areas of hydrothermal 13 - porphyry copper

2. Şumuleu, 3. 4. Ivo-Cocoizaş) (a); Porphyry-like alteration ± mineralization (5. Călimani, 6. 7. Jirca, 8. Vârghiş, 9. 10. Sântimbru (b); 14 - metal occurrences (II. Dornişoara, 12. 15 - sulphur occurrenees: a) (13. Negoiu b) minor (14. 16 - cinnabar oecurrences (15. 16. Băile 17 - c1ay minerals deposit (17.

18 - iron ore (siderite) occurrences: a) major occurrences (18. Mădăraş, 19. Lueta-VIăhiţa); b) occurrence area.

is a proving the existenee several types of hydrothennal processes (Stanciu, 1984): 1) porphyry systems to intrusive

processes, hydrothennai processes related to fractures, 3) postvolcanic activity, and 4) geothennal anomalies to weak meteorie-hydrothennal mineralization. Information on the Călimani-Gurghiu-Harghita ehain is quite recent and, in places, incomplete to the faet the surf ace observation is limited by scarcity of outcrops; works especially that only at several locations 1,200

Postmagmatie hydrothennal processes were focused in the infrastrueture of volcanic ........ u'"",,,,, and they induced transforinations within the prevolcanic (intercepted in boreholes at and Şumuleu struetures), voleaniclasties and, mostly, stratovolcanic assemblage (Peltz et 19981, 1982).

alteration and mineralization were eontrolled by subvolcanie intrusions (andesite andlor or granodiorite/dacite) loeated at different

of the stratovolcanic edifices. are especially loeated inside the craterial and caldera areas where the intrusive processes took the building up of the volcanic edifiees end ofthe eruptive

most representative process developed in the Fâncel-Lăpuşna (Lepeş zone), Şumuleu, Ostoroş and Ivo-Cocoizaş are located the major tectono-magmatic all~~lent (Peltz et 1976; Staneiu, 1976, 1977) (Fig. 29). Considering alI the paragenetie u.:>!.""".(L.;) (very complicated due to metasomatic interferences in the multiwintrusive spaces and the superposition of the and products), a zonal development of hydrothennal products on the generating intrusions can be observed. The suceession is: biotite - amphibole- chlorites - argillie - tourrnaline alteration. The biotite alteration, and subordinately the amphibolie one, both with innennost position, fonned the ...... :&l .. ,"'u'"' phase on an initial propylitie (autometamorphic type) background that in preserves small of fresh The subsequent alterations are the result of hydrothermal fluid that gave to transitional roeks and by eontamination with

64

------Volcanoclastic

formation

+

... + +

+ ... + ... + ... ... + +

+ + +

... +

...

...

+

~ ____ 1-.-:-:----:-:----:--

\Alteration mineralization-limit . \ of the porphyry ,---

I - I

1 I f I

... + + + ...

+ ... ... ... + ... + + .........

+ + ... Subvotcanic body ...

Fig. 29 - Hypothetic sketch showing the succession ofthe hypogene IJ"J ......... '...,

chain (ace. to Stanciu, 1976).

argiHic alteration mostly occurring within the host the porphyry alteration is completed in

the Gurghiu Mts while in Mts the hydrothermal process continued with an intense tourmaline metasomatism accompanied by formation of tourmaline-quartz veins (Peltz et 1982a; Stanciu, 1984). There is not evidence but it is tbat such formations may represent the final moments of the breccia pipe structures that are commonly u..:)'l,v"",,,,.,,,y to copper mineralization located within stratovolcanic edifi,ces, in the Andine Cordillera in Chile and Argentina (Sillitoe, Sawkins, 1971). .

metallic occur as disseminations, fissures and blurred veinlets being alteration However, a metallization was

observed in the propylitic zones, too. Pyrite is aU alteration zones the magnetite-pyrrhotite-chalcopyrite is associated the internal As the copper content is low, no zones interest outlined zone the metallic paragenesis is much simpler with pyrite as the characteristic mineral. tourmalinic rocks contain pyrite with or without marcasite, sporadically molybdenite or

Late-stage intrusive breccias formed certain fracture planes at Şumuleu and

65

the upper the porphyry-copper small vugs base-metal sulphide veins are frequently found. Lateral passage towards fissural deposition and ,",U'LUM""<-"

stibnite impregnations are observed at Ivo-Cocoizaş. Partial aspects ofthe porphyry-type alteration are recogIllz~:a Călimani caldera,

at Mermezeu, Seaca-Tătarca, Harghita-Băi (with near-surface ... ..," .... 'L ..... argillic rocks) and Sântimbru-Băi areas (Pe1tz et al., 1982).

hydrothermal processes related to postvolcanic tectonic activity appear generally at the exterior and upper part of porphyry a common alteration (propylitic-chloritic-argillic) took around the endogenous and breccias with base-metal and gold somewhat similar situation Îhas been encountered at

(NWof Mts.). In Sântimbru-Băi and Ivo-Cocoizaş zones the alteration is and argillization accompanied by superposed carbonation and "U'LV"',",,,,,,,,,,'U ± tourmalinization are prevailing (Vasilescu, 1 Peltz et al., 1974).

Numerous minor areas with poor indications of are controlled by non-mineralized fractures and zones of brecciation surrounded by argillic passing to silicic hatos following circulation pathways. areas the part of hydrothermal processes with still continuity at depth. Harghita Mts. This type is to volcanism in Călimani Harghita Mts. In Negoiu Românesc area caldera solfatara-type, exhalations interacted with local aquifers giving to native sulphur and limonite deposition conformable the stratification the pile. The sulphur concentrations occur as lenses and In a silicification aureole formed in andesitic pyroclastics. Massive sulphur is' associated pyrite, melnikovite and marcasite; subsequently, a less association consisting limonite, goethite hydrogoethite the sulphurlsulphide (Mureşan,

1969; 1984). , westem and eastem parts of the Călimani-Gurghiu-Harghita Mts contain

numerous small iron (siderite) closely to volcanoclastic formations (Mureşan, 1981; Peltz et 1982; lanovici et aL, 1983). Among two accumulations are located at Mădăraş and VIăhiţa. The mineral paragenesis displays low

"""AJ"VL"'jO,'~>J such as siderite ± Such types iron deposits, considered to generated under volcano-sedimentary or hydrothermal methasomatic conditions, according to (1992), represent a peculiar type of hydrothermal" Silica-saturated provided suitable

coprecipitation. At VIăhiţa-Lueta iron ore has been mined more 200 years and it is now

practically exhausted.

MetaUogenesis in passive margin-related settings

Restricted occurrences of Paleogene age are found at Căpuş (Gilău Massif, North Apuseni Mts) within epicontinental The ores are represented limonitic oolites found in carbonatic, and glauconitic cement (Vinogradov et 1963; Stoicovici, Mureşan, 1964). Such sedimentary ores were considered to formed on the north-westem passive continental margin the Transylvanian small ocean after unifitation of the

Apuseni island arc with the North Apuseni Mts block.

66

Sllear zone related ores

In the metamorphic rocks of the South Carpathians and to a extent in the Apuseni Mts are severa! ore occurrences of composition, always bearing or even gold-dominated, which can be ascribed to the shearzorte related ore type. The first approach was made by (1978, unpubl. data) in ascribing the

ores at Valea lui Stan, Căpătâna Mts to this ore types, at that named "tectogenic". Later on, the data were published (Udubaşa, Hann, 1988) and similar gold ores, Someşul Rece (Apuseni Mts), Jidoştiţa and Văliug (South Carpathians), have heen to belong to the shear zone related ores.

Productive shear zones, as describeg Udubaşa et al. (1 needing a protore to act as contain not only but also polymetallic ones (partly "pentametallic") (Figs. 31). Typically. shear zone related are the complex 6res of the

30 - Schematic representation ofthe gold protors from the central part ofthe South Carpathians, with the gold migration directions in the alluvial formatÎOns (ace. Udubaşa et 1992).

Key: 1 - Sebişel Series; 2 - manganiferous belt; 3 - nests oftitaniferolls hematÎte in quartz lenses; 4 - rocks rich in kyanite; 5 - blastomylonite belt; 6 - migration directions of gold from protori;; 7 gold concentrations (a - especially associated to the shearing zones: I. Costeşti-Horezu; II. Valea lui

III. Perişani; b - secondary-alluvial); 8 - research areal.

67

Fig. 31 -- between the fahlband-like ores (TT-Ţibra-Tâncava) + ND(Neguleţ-Dăniş) and the late (Alpine?) uranium mineralization (U pitchblende-thucholite) in the Leaota Mts., (ace. et

1992) Rocks arc Ca) micaschists and paragneisses with (b) sheared counter

Leaota Mts (considered to represent granitoidş by Vlad, ,LJ.u .... , ..

(1984), where both gold ores and ores exist andsometimes coexist in same spaee. The is qUÎte similar to of Skandinavian fahlbands. Further data on the Leaota and ore oceurrences are given by Udubaşa (1987, 1993), Lupulescu (1984) etc. It is to note that the the above-mentioned zones is of ages, Le. from Hereynian to Alpine, reworked by later .. "P· .... T'"

including ones (e.g. at brittle small-sized zones (SSSZ, ace. et al., 1998) epigenetic show always (mostly amphibolites) and highly discontinuous development of ore bodies or of zones. However, the content might locally

as high as 1 (e.g. Valea lui Stan).

MetaUogenesis in the post collisional-related settings

Burdigalian sandstones to Miocene East Carpathians comprise minor stratabound base-metal ores (sphalerite, galena, subordinate amounts

chalcopyrite) at (Săndulescu et 1988).

Miocene-Pleistocene heavy minerals accumulations (fossil placers)

By prospecting and exploration and by technologic studies, carried out in the most favourable situations, three areas with numerous accumulations

occurrences with heavy have been outlined: Getic Depression, the most important, Banat and Moldavian Platform (Panin, Panin, 1969; Panin

1988; Jipa et 1985) (Fig. 32).

68

1)..'\1.:(15

. - 6

~7 _ 8

~~. 9

Fig. 32 - Schematic distributian ofthe heavy minerals and alluvial gold accumulations in Romania. Key: 1 - Sedimentary cover ofthe Moesian, Scythian and East-Europe~m platfonns.; 2 - Carpathian orogen;.3 - North DOQrogean orogen; 4 - Carpathian foredeep; 5 -Intramontane depression; 6 -' Areals with occurrences and (a) accumulations of heavy minerals (Ti-Zr+-Au); 7 - Areals with occurrences and (a) accwnulations of alluvial gold. Representative accwnulations: 1. Glogova-Baboieşti-Ohaba-Şişeşti; 2, Malovăţ-Hinova; 3, Mateeşti-Alunu; 4, Râureni; 5, Gemenea-Tigveni; 6, Mâzgana-Onceşti; 7, Mugeşti-Igeşti; 8, Bursucani-Zorileşti-Pogana; 9, Iana­Corodeşti; 10, Codăieşti-Micheşti; 11, Scheia-Tăcuţa; 12, Chituc; 13, Perişor; 14, Ivancţla-Lumina-Rusu; 15, Sf. Gheorghe-Buhuz; 16, Cardou Sfistofca; 17, Ditrău; 18, Cibin Olt; 19, Pianu; 20, Comeşti-Mihai Viteazu; 21, Arieş Valley; 22, Haţeg; 23, Caransebeş; 24, Bozovici.

69

D 2 ~3 4 5

6 --7. 8 9 ____ 10

33 - showing the Sulina paleo-delta evolution and the formation of Sărăturile as well as the genesis ofthe mineral concentrations in the latter to Panin, Panin, 1969).

The figures 1, II, IV underline the Sulina paleo-delta retreat and the simultaneous progression of the Sârăturile formation.

Key: 1 - Accumulation formations (Letea-Caraorman) and older isolated lîttoral 2 -Sărăturile accumulation formations and their Iittoral bars; 3 - minerals concentration; 4 -meandering zones of Sulina and Sf. Gheorghe arms; 5 - marshes and lakes; 6 - limits gf the formation to accumulation and isolated fossil bars; 7 - lines showing the shore evolution; 8 - Iimits of meandering zones of the Danube arms; 9 - present-da)" shore; 10 - offshore currents; Il - movement of the shore-line (eros ion, accumulation or equilibrium, transient sedimentation).

70

Getic Depression, the Jiu, Olt, Argeş Dâmboviţa tbere is an important potential of heavy mineral concentrations, identified or outlined by exploration works and tecbnologic studies. Such concentrations are disposed at several levels at

part . Pontian the of the and occur as in tbe Dacian upper horizon. The mineralogical composition is, in general, 'similar; the common

of: amphiboles, garnets, magnetite, hematite, rutile, brookite, titanite, anatase, zircon, staurolite, apatite, kyanite, epidote, xenotime, monazite, titanomagnetite. Among the heavy minerals, ilmenite represents between 60 and 90%; zircon is represented mainly by The accumulations also monazite, quantitatively better represented. In most cases gold is found as well. Among the most important accumulations one may Glogova, Boboieşti, Ohaba-Şişeşti, Mateeşti-Alunu, Malovăţ-Hinova Tigveni 32).

In several occurrences been identified, similar with those in the Timiş Valley basin, between Orşova, Caransebeş and Lugoj. The association of the

minerals determined concentrates as follows: ilmenite, gamets, zircon, stauroIite, apatite, rutile, titanite, tourmaline, epidote, hornblende (Fig.

Similar accumulations of heavy minerals, with a significant geological potential, are known the Moldavian m zone between Prut most representative accumulations are: Mugeşti-Igeşti-Bursucani, Pogana, Corodeşti, Codă~şti-Micleşti, Scheia-Tăcuţa. presence zircon concentrates has

pointed out at sandy of Kersonian, Meotian Pontian-Dacian most cases higher contents of (up to 0.2%), în comparison with other

accumulations, been (Fig.

Recent deltaic and littoral accumulations

Danube is located between Moldavian Platform in Nortb and Dobrogean orogen in the South. The heavy mineral concentrations resuited by successive removal deposits and the sand (Panin, Panin, 1969) 33). It is noteworthy that mineral enrichment occurs in important erosion areas,

the fraction predominates where sands have accumulated. The oldest levels south-eastem Caraorman formation correspond to the Phanagorian

(3000-4000 years ago); they were formed by erosion SE Gheorghe 1 delta and the promotion of Sulina The level to Letea formation is younger (1000 it affected the Sulina Phanagorean delta while the Chilia delta progni:ssed towards minerals zones are exposed in southem Caraorman formation, and the Sărăturile and sandbanks. heavy mineral fraction consists gamet, ilmenite, magnetite, zircon, rotile, titanite, monazite, epidote, staurolite, kyanite, tourmaline, apatite, amphiboles, sillimanite, and chromite. The Hmenite, zircon, magnetite and rutile contents are of commercial Înterest The distribution is fairly sporadic; in the Caraorman formation it between 2 and 150 and in the Letea formation between and 50 The

and Chituc sandbanks contain major concentrations, 3-4 km long north of Sfântu Gheorghe; they occur along the Chituc zone. Heavy accumulations kg) inland margin. external of Caraorman and Sărăturile

71

sandbanks 90% The bottom alluvium and the suspended ...... '4".''11' .......

Danube Delta contain 2-12 kg/t of minerals.

Subactual and actual alluvial mineral and gold accumulations

The of the researches pointed out that numerous hydrographic basins the rivers Romania contain heavy minerals accumulations (Ti, bearing) and

gold with a variable distribution, whose economic significance is to be determined (Jipa et al., 1985; Panin et 1988). It is to note the actual alluvia aUuvial terraces with

contents of identified in the Bozovici-Caransebeş-Orşova, basins, Pianu zone Transylvania Basin, Olt, Jiu-Argeş rivers area and Gemenea-

Târgovişte in the Depression, Comeşti-Mihai zone (Turda), Drăganului VaHey-Poieni-Morlaca zone in Apuseni Mountains and Ditrău (Fig.

Heavy minerals accumulations are also included in the sediments .;)f storage at Porţile de which a quantitative prognosis has been determined, and at Bicaz.

The quantified metallogenetic analysis Îs focused on the assemblage the metaHiferous mineral resources with the total mineral potential (TMP) evaluated in metal tons and/or per on types substances, which cumulates, according to the systematics adopted by the reserves (exploited + actual) and resources (Borcoş et aL, 1997), corresponds to made the

ommu[{cc (1997) conceming The potential is a150 rendered evident by of ore deposit, in agreement with norms used by the Commission on the Geological Map ofthe World - Sub-commission on Metallogenetic Map, thus establishing their within the metaHogenetic units representative the Romanian territory (Table 12).

TABLE 12

SIZE OF THE BODIES (DEPOSITS/PROSPECTS)

SUBSTANCE LIMIT BETWEEN THE SIZES (metric tons metall 2 and 1 3 and 2 , 4and 3

Pb ar Pb+Zn 50,000 1,000,000 4,000,000 Cu 50,000 1,000,000 10,000,000 Au +/- Ag 10 50 500

,Ma 5,000 50,000 200,000 Mn 500,000 5,000,000 100,000,000 Fe(+-Mn); Fe-TÎ-V 10,000,000 100,000,000 1,000,000,000

1 - small ore rtA",nC::'ltc::: 2 - medium ore depasits; 3 - large depasits; 4 - very depasits

72

The metallogenetic based on: (l) the assessment of mineral potential including non-ferrous ores Cu < OA %), ores and ferrous-ores Mn, Fe < 15 %, Ti-V), (2) relation of ore deposits to plate-tectonics . (Cioflica, Vlad, 1984; 1986; Rădulescu et al., 1994; Vlad, Borcoş, 1994, 1997) and the modelling studies

The metallogenetic study only to the global accumulations of their mineability or non-mineability) estJlmated (metal tons and/or per cent), which includes reserves (exploited and/or existent) and resources.

u\.., .• UL'''' ores which, as a matter are best represented on the territory, substances that can also be ·'lentioned (especially uranium, molybdenum, tungsten, mercury, nickel) due to the volumes have not in the analysis as carmot change substantially value of the estimated TMP.

main preliminary conclusions information about preferential location accumulations in districts according to metallogenetic space-time evolution, about the metallogenetic specification, on the geotectonic units, about the anc} geologic processes and about the geographic units; the assessment of the of on geologic processes and the share of the within the yielding sources and.processes.

analysis methodology possible the the existing reserves resources to tridimensional

scheme of representation of the technological and economic features, recently adopted by the Economic for Europe (United Nations) (Figs. 34, 35). determined for the types of ores permit a clear differentiation of the economic reserves from the non-economic ones and take into consideration the position of the reserves whose and economic

are to be better The results obtained the base-metal, gold-silver and ores confirm, for the main ores deposits, ore deposit

mining fields), geo-economic same can contribute to the

estabIishing of the policies and development fundamental aud applicative surveys (geologic and technologic) aud mineral resources.

Space-time distribution and global estimation on metallogenetic districts (Plate II, Table 13)

metallogenetic V .... ~4'U'U of Romauia's t"" ...... f(u ... , is associated with major intervals, one with a distinct and metallogenetic

"'p."."u,u ... _~ •. v .. which corresponds to: non-differentÎated cycles 49.54 %, CaleaOnJlan cycle 4.34 %, cycle 9.89 % and Alpine 36.0 %; the

accurnulation replreSiefl1rS only 0.89 %.

I The values mentioned in the text for the various units, types and corresponding to the whole territory of Romania.

processes are referred to TMP,

QUANTIFIED PROVED PROBABLE

ll\ k.p.R.\ '1\

'1\ fi·p·R. \ I I \

, . , I " . . . . : p.R. " • I • · . · . o • , . ... I : . . . . .. p.P.R. . . 0'1 " . . . .

UNQUANTIFIED POSSIBLE

u

~ \ I I ~ \m.r.! ps.r. ~ \ I ~~~~~ __ -L __ ~~~ __ ~ __ ~~~ __ -L ______________ ~~

DEGREE OF KNOWLEDGE

TRANSPOSITION OF THE ACTUAL STRUCTURE OF TIU: MINERAL POTENTIAL IN THE PROPOSED CLASSIFICATION SYSTEM

O Reserve from group audit partially inadequately placed

1\ « ) Reserve from group out of audit and unclassified. partialJy cumuJated V .

• ' '. Progllosis reserve (Pl ± P2), partially cumuJated andlor inadequately placed .. . CORESPONDENCES

i.R. + i.r. - Reserves and resources of immediate interest m.R == A + B + CI - reserves from group of audit i.R. = C - reserves in extensîon of ilie audil reserve p.R + p.r = P, ± P2 - prognosis reserves

P.R + p.r. - Reserves and resources of perspective m.P.R. = B + CI - reserves from out of audit

= CI - unclassified rescrves i.P.R. = reserves in extension of reserves out of audit

= C 2 - unclassified reserves p.P.R. + p.P. = PI ± P2 - prognosis reserves

r - Resources m.r. '" B+ CI - reserves from out of audit

== CI - imclassified reservcs Lr. == rescrves out of audit

== e2 - unclassified rcservcs p.r. + ps.r. == PI ± P2 - prognosis reserves

Fig. 34 - System of reserves and resources c1assification and reconversionof the mineral potential from the alpha-numeric system in the system adopted by CE-ONU.

73

74

a:: l-V!

..J <{

1-Z I.IJ

a..

Q) >

"51 :J

C· O -O O -I.IJ I.IJ O -O

"-O

E II) -II)

V!

E c :::J O o:;:;

O

,Q) V!

Fig. 3'

MP MIN AL POTENTIAL

RESERVES(mRESOURCES[R)

Geological

Ge~logical-technologiCal rl'search- economical ana'tysiS

>-1-

....J

ro «

m r. i r.

Ig t va ua Ion J

! CGPMRI. CONVERTED GEOLOGICAL POTENTIAL IN MEASURED RESERVESOF IMMEDIATE INIERESJ

1 2 3

rted CR"ri. Converted C r. Conveded reserves and reserves and resources resources of resources of

immediate interest immediate interes

Te chnological . valuation ~

CGPWR CONVERTED GEOlOGICAL POTENTIAL IN IWORKABlE 1 RESERVES WHICH COUlD BE INDUST RIALlZED

1 J 1. l 3

Economic valuaiion

CGPSP. CONVERTED .GI OLOGICAL POTENTIAL IN

SA LEABLE PRODUCTS L 1 I 2 1 3

ECONOMIC -MARGI~~ ECONOMIC

1 I 2 I 3 ·UNDEFINED NOECONOMIC

ofanalysis and promotion ofthe potential

Table 13 Systematics of the geological potential distributed on geotectonics cycles, geological processes and metaUogenetic districts/zones

GEOTECTONIC GEOLOGIC PROCESS - DISTRICT (O) No. Geo- Genetic COMMOolTIES Potential O Of Z r.te".d to: Size of ~

graphic types2 Genetic Geo-tect CYClES ORE BEARING FORMATIONS ZONE (Z) Total accumula-

(0,4 lotal potential) (% referred to eyele; ",4 referred to total potential) units' process-% cycles-°,4 potentlal-°,4 tlon.'

CYCLES Metamorphie fonnalions (Ptz,) D. Palazu 1 SD 11(8) 100 Fe. 100.00 77.08 38.18 12 PROTEROZOIC Carbonatie, amphibo/ic and micaeeous fonnations (Ptz 2 -3 ) D. Valea Blaznel·Guset 2 E.C 11(9) 96.48 Pb+Zn; 0.07 Cu; 3.44 Fe. 2.83 0.65 0.32 cl-2

NON-OIFFERENTIATEO 22.92',4 D. Bazdaga 3 E.C 119) 87.38 Pb+Zn; 12.62 Cu. 0.01 0.003 0002 cI 49 .54% 11.35% D. Razoare 4 E.C 119) 50.48 Mn; 49 . ~ Fe. 43.06 9.87 4.89 b2

Z . East Carpathians 5 E.C. 119) 90.59 Pb+Zn; 9.41 Cu. 0.23 0.05 0.03 el D. Porumbacu-Arpas 6 S.C 119) 91.36 Pb+Z"; 8.64 Cu. 0.10 0.02 0.01 cl Z. Banat·Muntii Sebes 7 S.C. 11 10) 31.46 Fe: 68.54 Mn 46.48 10.65 5.28 b2 D. Delinesti-Tamova 8 S C. 11 10) 87.80 Fe; 32.20 Mn 5.88 1.35 0.67 al D. Toplet 9 SC. 11(6) 52.20 Fe: 47.80 Mn. 0.65 0.15 0.07 al D. Valea Fierulul-Boutari 10 S.C 11(6) 100 Fe. 0. 16 0.04 0.02 al D . Annenis 11 S.C. 116) 100 Fe. 0.27 0.06 0.Q3 al D Altan-Tepe 12 CD. 11(5) 100 Cu. 0.32 0.07 0.04 dl

CALEOONIAN Extensional submarine basic volcanism (Ptzl-Cb,) D. Silvas-Boita-Lingina 13 SC. 11(5) 100 Pb+Zn. 68.11 0.96 0.04 cI 4.34·,4 1.44",\,; 0.06',4 D. Boclugea-Camena 14 N.D. 1.1(5) 1.23 Cu: 98.71 Fe. 31 .69 0.46 0.02 al

Rhyolitic volcanism (Cb) D. Baia Borsa 15 E.C. 11(5) 84 .61 Po+Zn: 15.30 Cu; 009 Au+Ag . 65.15 19.50 0.85 el-2: dl 29.93·'\' D. Fundu Moldovei-Lesu U~ului 16 E.C 115) 45.33 Po+Zn: ~.64 Cu: 0.03 Au+Ag 14.37 4.30 0.19 el : dl 1.3% D. Cartlbaoa-ooma·Anni 17 E C. 11(5) 88 .67 Pb+Zn: 11 .33 Cu 3 27 0.98 0.04 el

D. Balan· Tulghes 18 E.C 11(5) 1704 Pb+Zn: 82.96 Cu 16. 74 501 0.22 el ; dl D. Comana-Venetia 19 SC 11(5) 100 po+Zn. 0.47 0.14 0.01 el

Graphitous fonnat ion with Iydites (Cbl D . Vatra Domei 20 E.C. 11(9) 30 22 Fe: 69.78 Mn 100 00 68.63 2.96 bl HERCYNIAN Volcano-sedimentary tonnations of extensional type (SI D. Anies 21 E.C 11(6) 10e Cu 0 22 0.001 0.0001 dl

9.89% 0.49°,4; 0.05',4 O. Rusaia 22 E.C. 11 \5) 100 Fe 99 78 0.49 0.05 al Submarine basic volcanism (O) D. Teliuc-Ruschita 23 SC 11(5) gl69 Fe: 6.11 Mo. 8/' .21 8529 8.44 al

97.7S',\,; 9.U',\, D. lazuri-Cerbal 24 SC. 11(5) 100 Fe. 12.79 12.51 1.24 al Rhyolitic volcanism (Lower Carboniferous) O. Muncel-Rapolt 25 SC. 11(5) g5.74 Pb+Zn; 4.21 Cu ' 0.05 Au+Ag 100.00 1.71 0.17 el-2: dl

Granitic magmatism (P) D. Soimus-Dud 26 A.M. 11(5) 100 Cu 100.00 0.001 0.0001 dl UNCERTAIN PRE-ALPINE Aeeumulalions with uncertain souree and posltion Z. W. Zone of South Carpathlans 27 SC 11(5) 87 .36 Fe; 13.64 Mn. l CoaCOI 100.00 , 0.22 b2

ALPINE Mesosoic carbonatic fonnations O. Moneasa 28 AM 11 (5) 73.42 Fe: 26 .58 Mn 100.00 3.56, 1.29 01 36.00% Oetritial fonnations (Jl} D. Valea Mare-Suncuius 29 AM . 7 100 Fe. 100 .00 0.13 0.05 al

otwhich: Marine tonnations (Cr) D. Campulung MOldovenesc 30 E.C 8 100 Fe. 100 001 0.26 0.10 al Exogenous Epi.:ontinental fonnations (Pg) O. Capus-SavadisJa 31 T.B. 8 IOD Fa. 100 001 8'40 304 al

12.43";' of lotal Alpine Rifting (bimodal T,.J, - N.D.; alkalin. J,.JI - E.C.) D oitrau 32 E.C 4 100 F~ 95 45 ' 42.70 15.47 al EndClgenous 45.02%; 16.21% D Somova·Marca 33 N.C 13 95.16 Pb+Zn. 4.8C Cu 004 Au+Ag 0 29, 0.13 0.05 cI

31 .53"'\' of total potential D. lulia-Eschibalac 34 ND. 2 99 .45 Fe 0.3i' Cu 0.18 Mn " 25 1.91 0.89 al

Spreading - tholei itic assoc. (T z.J l ) D. Baia de Arama 35 SC 5 100 Cu 100 0C 0.02 0.01, dl

Island arc magmatism - tholeiitic assoc. (JI-Cr, ~ O orocea 36 AM . 5 18.44 PO~Zn 61.56 Cu 0 21 ) 00121

0.004 dl

5.63',4 4 8299 Fe: 16 ~4 TI O 37 V 9 1 4S 1 5. 11 · 185 al 2.03% D. Techereu 37 AM. 4 90 .91 Fe: 9.09 Ti. 001 022 008 al

D Pamesti 38 A.M. 6 100 Mn O 10 ' O OI 0.002 01

D. Vorta-oealul Mare 391 A.M . 5 94 .77 Pb"Zn: 5.23 Cu. 4 21 024 0.09 cI

Banatitic magmatism - c.lc .. lkalin. assoc. (Cr2-Pg, ) O. Moldova Noua-Sasca 40 SC 2 7.13 Po+Zn: 40.69 Cu: 0.002 Au .. Ag: 46 .03 re ; 015 Mo. 14.591

2.20 0.60 cI : dl

IS.2',\, 3 98.33 Cu: 1.67 Mo. S 07 017 028 d2 5.47',\, o . Oravita 41 S.C 2 83.10 Pc+Zn; 16.74 Cu: 0.01 Au+Ag: 015 Mo. 0.50 008 0.03 CI: dl

3 100 Cu 013 002 0.01, dl

O Ocna de Fier-Oogneeea 421 SC 2 1.61 Po+!n; 0.49 Cu: 0.001 Au+Ag: 96.68 Fe. 1.22 Mn. 32 .26 4.87 1.71 al : el

D. Tinccva 43 SC 2 11 .64 Pb+Zn. 88 .36 Cu : 0.001 Au. 0.09 0.01 0.01 el : dl

O. Ruschila 44 SC. 2 100 Pb+Zn. 0.12 0.02 0.01 el S.C 1 99.41 Po+Zn : O 57 Cu : 0.02 Au 182 0.27 0.10 el

O Bocsa-Hauzesti 45 SC. 1 72 .22 Pb+Zn: 27 .78 Cu. 002 0.004 O.COI el

D liliecl-lapusnlcul Mare 46 SC 3 97.20 Cu: 0.01 Au+Ag. 2.79 Mo. 026 0.04 0.01 dl

D Poiana Rusea 47 SC 1 99.99 Cu; 0.01 Au 0.06 001 0.003 dl

O Baisoara 48 A.M. 1 96 .57 Pb+Zn; 3.39 Cu: O 04 ,1.g . 4.13 0.82' 0.23 CI

2 99.42 Fe; 0.58 Mn. 34 50 523 1.69 al O. Gilau 49 A.M. 1 99 .99 PO; 0.01 A~ 0.04 0.'01 0.002 el D. Baita-Hamagiu 50 A.M. 1 92 .29 Po+Zn: 7.48 Cu; 0.23 Au+Ag 0.14 0.02 0.01 cl

2 84.68 Pb+Zn; 15.30 Cu: 0.02 Au+Ag 2.14 0.32 0.12 el O. Budureasa-Valea ragului 51 A.M. 1 11 .09 Pb+Zn: 0.41Cu: O.OOlAu+Ag; 88.54 re . 2.27 0.34 0.12 a1. el D V1adeasa 52 A.M . 1 86.44 P!>+Zn; 13.50 Cu: 0.06 Au+Ag. O 14 0.021 0.01 cI O. Borod-Comitel 53 A.M . 1 95.21 Pb+Zn: 4.74 Cu: 0.05 Au+A\l 0.17 0.03 1 0.01 el D. Magureaua 'Ialei-Birt," 54 A.M. 1 99.72 Po+Zn: 0.25 Cu: 0.03 Au"Ag 0.11 002

1 001 cI

2 95 .21 Fe: 4.79 Mn 132 0 .2Q 0.07 al Neogene volcanism - calc..alkaline assoc. (m-pl) D Tarna Mare 55 E.C 1 95.03 Pb+Zn : 4.86 Cu : 0.11 Au+.A.g 3.95 0.80 0.29 el

22.48% O lIoa-Nistru 56 E.C 1 80.55 Pb+Zn: 1935 Cu: O 10 Au+AJl: 319 065 0.23 cl·2 : el 7.37% O Sasar·Valea Rosle 57 E.C 1 96.42 Po+Zn; 2.67 Cu: 0.91 Au"Ag. 041 0.08 0.03 cI

O oealu Crucii-Baiut 58 E.C 1 90.14 Po+Zn: 9 72 Cu: 0.14 Au~Ag . 18.75 3.82 1.38 el ; el

D. Huta-Ceneze 59 Ee 6 100 Fe. 0 29 0.06 0.02 el·2 O. Toroi.aga 60 E.C 1 59.78 po"'Zn: 39.98 Cu: 0.24 Au+Ag . 0.38 0.08 0.03 al D Tioles 61 EC 1 92.14 Po+Zn; 7.74 Cu: 012 Au+Ag. 0.29 0.C6 0.02 cl: dl D Rodna 62 E.C 1 77.97 po"'Zn : 1.37 Cu : 0.07 Au+Ag: 0.16 ,"'n. 2043 Fe. 2.S0 0.51 0.18 el O Cal iman, 63 E.C 1 97.66 Ptl+Zn: 227 Cu: 0.07 Au+Ag 0.11 002 0.01 el

5 100 Fe 10.35 2.11 0.76 el O Madaras 64 E.C 6 99.83 Fe: 0.17 Mn 19 03 3.6/' 1.40 al D Lueta-Vlahita 65 E.C. 6 9809 Fe: 1.91 Mn 6.82' 1.39 0.50 al

D Toplita·Ciuc 66 E.C 6 96.77 Fe 3.23 Mn. 7.44 1.51 0.55 al

O. Rosia Montana-Contu 67' AM 1 100 Au+Ag 0.02 0.005 0.002 el-2 D. Baita-Cainei-Draica 68 1 A.M 1 100 AU+~\l O.GOC4 1 O.OCOI 0.00003 el-2

O Baia de Anes 69 AM 1 97.29 Po+Zn: 2.52 Cu: O 19 Au+~ 047 0.10 0.03 cI : el O Buclum-Rosia POle'1! 70

1

A.M 1 81 .31 Po+Zn: 17. 12 Cu: 157 Au+Ag 0.05 001 0004 el 3 99 .50 Cu: 0.07 Au+Ag: O 43 Mo 18 15 3.69 1.34 d2

O Zlatna-Stanlja I 71 A.M 1 99.82 Po"Zn: 0.18 Au+Ag ~ ;7 1 0. 11 0.04 cI: el

I 3 99.78 Cu: O 22 Au+Ag 0.47 0.17 d l O Brad·Sacaramo

I 72

1

A.M 1 98.32 Pb+Zn. 0.70 Cu: O 98 Au+ Ag. 2 0' 1 041

1

O 15/ cI : e2 3 99.85 Cu: 0.15 Au+Ag 2.03 0.41 015 dl

D. Deva 3 A .M . 3 100 Cu 0.34 007 0.03 dl

O Talagiu 741

AM 1 99.43 Pb+Zn: 0.57 Au+Ag. 0.07 0.01 0.01 el 3 100 Cu 0.50 0.10 0.04 dl

Cotlision (?) O. Nimaia-V Lucului 75 S.C 12 99.99 Pb+Zn: O.OOIAg. 0.51 0.01 0.002 cI 1.15% D. Valea lui Stan 76 SC 12 100 Au+Ag. O.OeOOl 0.00001 0.000003 81-2 0.42°k Z East Carpalhians 77 E.C. 13 1.35 Pb+Zn: O 62 Cu; 0.003 Ag: 96.98 Fe: 1.03 Mn. 98.88 1.13 0.41 al ; el

D. Somesul Rece-Munte'e Sacel 7/3 A.M 12 100 Au+Ag. 0.Oe05 0.00001 0 .000002 el D. Lupsa 79 A.M 13 100 Cu. 0.44 001 0.002 dl D. Ranusa-Zimbru 80 A.M 13 100Cu. 0.36 0.004 0.001 dl

Accumulations with uncerta in source and posilior1l O. Cioclovina 81 SC. 13 100 Pb+Zn 15.91 0.02 0.01 cI 0. 10'~ ; 0.04% D Valiug-Sozoviei 82 S.C 13 100 Au+Ag. 0.029 0.00003 0.00001 81

D Rametea 83 AM . 13 92.11 Fe: 7.69 Mn . 84.06 0.08 0.03 el

1 _ EC - East Carpathlans: SC - South Carpathians: AM -Apuseni Montains; TO - Transylvanian oepresion ; SD - South ooorogea. Co . Central Doorogea: No . North Dobrogea 1 _ 1. Hydrothermal : 2 Skam ; 3. Porphyry; 4. Orthomagmatic: 5. Volcanogene; 6. Voleano-sedimentary: 7. Residual: 8. Chemieal preeipitation: 9 Assoeiated tO carbonate rocks ; 10. Associated to silieiclast rc rocks: " . MetamorpMsed: 12. Tectogenous; 13 . Polygenetic - remobilised 3 a - iron, b - mangan, c· lead ~ zinc, d . copper, 8 - gold + argent

Claasl-

fication

DorZ

1

24 75 5

55 112 4

20 41 80 51 48

45 59 17 31 46 29 tl6 7

78 42 3

15 33 79 28 14 44 37 ti 2

43 19 64

9

39 72 36 16

50

10 68 36

71 61 69 6

70 34

35 65 63 40

26 27 52 12 58 54 57 32 18

11 22 21 74 60 49 13

30

25

56 47

71 62 23 63 73 76 87 81 53

75

The non-differentiated Proterozoic cycles include mainly iron and manganese accumulations, and subordinately lead-zinc ones occurring in two formations: the former, Karelian metamorphic formations (PtZl) (38.18 %) and the latter, carbonate~ amphibolic and micaceous formations (PtZ2-3) (11.35 %). Most of the potential distributed in the Palazu district is represented by iron mineralizations. The accumulations related to the carbonate, amphibolic and micaceous formations (PtZ2-3) are spread over Il districts or metallogenetic zones in the South and East Carpathians and Central Dobrogea, of which, from the TMP point of view, the most important are: Banat zone - Sebeş Mts, as well as Răzoare, Blazna Valley and Delineşti - Târnova districts. Most of the potential can be referred to the iron and manganese accumulations, and only to a lesser extent to the lead­zinc accumulations. The size of ore deposit, except those at Palazu, Sebeş Mts, Răzoare and Blazna Valley which are of a medium size, ranges within the limits accepted for smaH-sized accumulations.

As regards the mineability of the ores, regardless of the composition types, it is to note that the majority of the accumulations within these cycles are hard to be mined (situated at shallow depths, low contents, high degree of accumulations spreading) or un­mineable.

The Caledonian cycle includes accumulations (mainly lead-zinc, copper and manganese) which occur at three geological levels; the order of the TMP these are, as follows: graphite formation with Cambrian lydites (2.98 %), Cambrian rhyolitic volcanism (1.30 %) and extensional submarine basic volcanism (Ptz3 - Cb l ) (0.06 %), respectively. In general, the accumulations have a simple composition, which includes either manganese ores (±Fe) (graphite formation with Cambrian lydites) or lead-zinc ores (± copper, ± gold) (Cambrian rhyolitic volcanism and basic submarine one PtZ3 -Cb l ), or copper (± lead ± zinc) (Cambrian rhyolitic volcanism). The major districts are in the East Carpathians at Vatra Domei (manganese ore), Baia Borşa and Fundu Moldovei - Leşu Ursului (lead and zinc ore, beside copper and subordinately gold). As regards the size of the ore deposit, most of the accumulations are small-sized, except the ore deposits from the Baia Borşa district (Dealul Bucăţii - Cornul Nedeii and Gura Băii -Măcârlău - Ivascoaia - Novicior ) which are medium-sized.

The mineability of the manganese ofes is reduced due to the low contents and to the high degree of spreading of the mineralizations, while the lead-zinc ores raise several problems particularly as regards the technology of recovery of the metals and the obtaining saleable concentrates (e.g. in the districts Baia Borşa and Fundu Moldovei -Leşu Ursului).

The Hercynian cycle contains various ore deposits (iron, lead - zinc in copper) located in several geological levels, as follows: Devonian sub-marine basic volcanism (9.68 %), Lower Carboniferous rhyolitic volcanism (0.17 %), Silurian extensional - type basic formations (0.0001 %) and Permian granitic magmatism (0.0001 %). The most important genetic units - districts - are related to the Devonian basic volcanism with iron mineralisations (to which manganese is also associated in small amounts) (Teliuc -Ruşchita district, the third one as regards the value of the potential), as weB as to the Lower Carboniferous rhyolitic volcanism with lead-zint mineralisations (to which copper and in places gold are associated) (Muncel- Rapolt district). With one exception

76

(the Muncellead-zinc ore deposit of medium size), all the other accumulations are of small

the mineability, majority of the accumulations small contents of metals.

small-sized iron Carpathians, which .. ",,,, ... ,,,,,"'t'l1"

Alpine source position are unknown.

accumulations occur in 0.22 % of the Dotlennal

,.." .... ,.""... cycle ""VJ'UQ,UI~ .. ...,"yIJllyIU .. 'V' with the ore composition related to several both types copper, gold, iron and mangIJme1;e

exogenous and particularly endogenous ones. r'Lu'V1J,~ the exogenous (4.48 %), mention of

the accumulations related to the epicontinental forrnations (3.04 %), with higher of the TMP, and the marine formations (0.10 %), and the Jurassic formation~ (0.05 %) with values of the TMP. Generally, the

nr()Ce:SSf~S are characterised by iron accumulations manganese). endogenous mineralisations represent 31.53 % which could be put in

,,"' ...... ,,' .. with spreading, island arc, subduction and collision geotectonic and

major metaUogenetic are, as foUows: bimodâl and alkaline rifting magmlansm ( J3; J I - J3) (1 subduction related to the volcanism (m pl) (7.37 %) ,and to Banatitic (Cr2 - Pg1) (5.47 %), to collision (?) (0.42 %) or to spreading processes (T2 J3) (0.01 %); some have an source and position (0.04 %). Within the in most complex lead-zinc ± Au , Ag), copper Pb, ± Au ± Mo), gold (gold silver) ( ± Pb, Zn , Cu), iron (± Ti,U) and manganese accumulations formed.

,.pnr", .. ri" the size of the ore the accumulations are small-Medium-sized ore deposits are rarely found, e.g. gold accumulations at Barza and lVlOinUlllla. or lead-zinc at Ghezuri - Penigher, Băiuţ,

From the point the mineability, most accumulations related to the Alpine cycle are are, however, such as those related to a part of the iron accumulations (particularly the ones which are difficult to mined or are among the accumulations, the orthomagmatic ones are difficult to mined or have low and the volcano-

ones are worked out or with low contents), accumulations (espeeially related to the proeesses or to source aud position), and accumulations (related to shear zones with uncertain souree and position).

Small Au-Ag accumulations Pb-Zn and Fe-Mn occurrences the South the Apuseni Mts on1y 0.10 % of the TMP, their Alpine

being' uncertaÎn.

77

Taking into account the of the main accumulations and occurrences in Romania, a picture of different mineral associations OF was established as shown in (Udubaşa, 1992). Some minerals by their main elelllents) have formed practicaBy during the whole time interval since the Precambrian tiU i.e. iron-, copper, lead-zinc- and calcium (mostly calcite)

a enrichment certain time such as of Mo, Mn, etc. Finally, there are time-bound mineral assemblages, i.e.

minerals of Au, Ag, Sb, Regarding the species number, the richest mineral-forming are related to the Neogene igneous activity, producing locally clear and remobiliz~tion of some elements from basement. conspicuous are such processes in Northern Romania (Baia Mare where abundant rhodochrosite appears associated with important vein sulphide assemblages Cavnic ore deposit, 1978). Much more complex seem to be the remobilization

Metaliferi Mts., where a geochemic.al triad, Le. Au-Te-Mn, has in connection with the role of the (mostly ophiolitic) in

........ "' ..... 0 at least Mn, not Au and too (Udubaşa et al., 1985). same a area" (in sense of Routhier, 1977) rich in Mo has been found, which was repeatedly activated during Lower Cretaceous-Miocene time some molybdenite occurrences mostly along Mures zone.

Productivity of the ore _",."",,,,a,, and geologic processes (Tabies 14 and 15)

The most productive ore terms of TMP are the volcanogenic -sedimentary type with 66.36 % 'ofthem Mare deposit is 38.17 %), followed by orthomagmatic ores by Fe < 15 %) with 1 %. The metasomatic ores (skam distal replacement) types are 4.48 %, hydrothermal veins breccia pipe type is 3.71 %, porphyry copper types are % and exogenous ores are 4.48 %.

An metallogenetic approach commodities Pb-Zn, "" .... -" ... t::.. Cu, Fe Cu < 0.4 %, < 15 % is below.

Pb - Zn. The ore formation is widely distributed across the stratigraphic-time scale. "UIIJUJ,,,", and Paleozoic occurrences with 65 % 22.47 % of TMP. Tertiary subduction events yielded 15.26 % and 80.70 % the

Pb+Zn potential of the Alpine cycle. m~ important genetic type is hydrothermal - breccia computed as % TMP, followed by volcanogenic metamorphosed deposits with 30.87 % The deposits taken into consideration are commonly of small and medium size. Large deposits are represented by Cavnic-Roata and Sprie vein and volcanogenic deposit.

Cu. The ore formation shows a similar pattern compared to Pb-Zn occurrences. Alpine ores represent 58.12 % TMP and Paleozoic ores 37.18 % The Banatitic and Tertiary subduction events yielded 66.36 % 32.63 % of the total potential the Alpine cycle. The most productive type Îs volcanogemc metamorphosed with 40.8 % TMP. Metasomatic types enclose 36.61 % TMP. Copper aetlOslts in Romania are of small and medium

78

CAIN

MEZOZOIC

PAlEOZOIC

PRECAMBRIAN

I I I I

Ti,

--,--I I I I

.. .. " "

, .. ..

36 - Schematic representation of different mineral groups P'Ylrlre;!:!:fl,l1 by their main metals to Udubaşa et al., 1992).

Table 14 Produetivity of ~ompo8itional of ~res aud ofyieldiug geological processes ORE TYPES GENETICj---":'::':"'::"';:":::;";;";:;"''''':':''-j

LEAC ZINC 4.36%

COPPER

1.16%

GOLD·SIL 0.01%

tRON 66.67%

MANGANESE '9.53%

COPPER (Cu<0.4%) 2.02%

IRON (Fe<15%1 17.42%

Alpine accumulations with uncertaln S1)UI"Ce arni posltion

Metamorphie fonnations (Ptz,)

Submarine basie volcenism D) Carbonatie, amphibolie and mlcaceous fonnatians (PtZ2-3)

Banalilic magnalism • calc-alkallne assoe. (CrrPg,)

osillon

2,4,13 1.05 12,13 0.61

13 0.29 8 0.15

0.04

'. 1. Hydrothennal; 2. Skam ; 3. Porphyry; 4. OrthomagmaUc; 5. Volcanogana; 6. Volcano-sedimentary; 7. Resldual; 8. Chemlcat preclpilallon; 9. AssocIaled 10 carbonale rocks; 10. Assoclaled to slilelelastic rocks; 11. Metamorphosed; 12. Tectogenous: 13. Polygenelie· remobllised. 2 a • iron, b· mangan, elead" zinc, d • copper, e • gold + argen! (siza of aeeumulatlon according to Table 13)

0.003 0.0003 0.0001

0.71 0.41 0.20 0.10 0.03

el el el el el

a2 al a1

a1 al al al al

b1

bl b1 bl bl

d1-2 dl-2

79

Table Productivity types of ores aad

GENETIC

TYPES

C% of total polllol:llli) HYDROlHERMAl

2.110%

SKARN

6.3t%

PORPHYRY

17.40%

VOlCANOGENE

0.116%

VOlCANO-8EDIMENTARY 2.48%

RESIDUAl 1.34%

CHEII/UCAL PRECIPITATION 3.14%

VOlCANOGENEMETAMORPHOSED

1.62%

VOlCAN0.5EDIMENTARY METAMORPHOSED

0.12%

CHEMICAl PRECIPITATION METAMORPHOSED 47.86%

MSOC. TO CARBONATIC ROCKS METAMORPHOSED IIJI3%

GEOTECTONIC

ALPfNE

100%

ALPINE

100%

ALPfNE 100%

ALPINE 100%

ALPINE 100%

NON.fJlFFERENnATED-2.27"

119.47%

GEOLOGIC PROCESS -

ORE BEARING FORMATIONS

magnatism calc-alkaline assoc. (Cr:rPg,) volcaoism • calc-ailleline IiISSOC. (m-pl)

"moda! T,..J, - D.N; alkalina J,..J3 • C.O)

magnatism calc-alkaline Issac. (Cr2'Pg,)

Bana/ilie magnatism calc-alkallne IISSOC. (CrrPg,)

Island arc magma!lsm - tholeiilic assoe. (J3,Cr,)

Spreading • Iholeiilie assoc. (f ~-J31

Islllnd arc magmalism -Iholeiitic assoc. (Jl-Cr,)

Neoaene volcanîsm • calc-alkaline assac. (m-pl)

Island arc magmalism ' tholeiitlc assoc. (J3-Cf,l Neogene volcanism - calc-alkaline assoc. (m-pl)

ICollision (1)

" EC, Easl Carpalhians; se· Soulh Carpath!ans; AM -Apuseni Mon/aIM: TD" Transilvanian Depresion: SD South Dobrogea. CO· Cenlral Dobrogea; ND· North Dobrogea 2. a, iron. b. mangan. c, lead zinc, d copper. e ' gold .. argenl (size 01 accumufalion accordong 10 Table 13) ,

F)

14.80 85.20

88.89

11.11

1.02

10.39 88.59

0.08

100.00 30.53 6.65

57.89 4.93

SIZEOF

ACCUMU-

<11-2

'a1

a1;d1

d1

81;d1 a1;e1;<1

b1 a1 b1

a1;b1

c1;e1 a1;b1

el al ;b1;C1 al;e1 :el

00 O

81

- Ag. Gold mineralization is intimately assoCÎated with the Alpine cycle that provided 87.41 % TMP. The subduction event yielded 85.38 % TMP epithermal systems and subordinately porphyry coppers. Barza and Roşia Montana are world class deposits and the rest are of small and medium

Fe. Iron metallogeny is characteristic of Precambrian to Alpine cycles, with ' special ~o Lower Proterozoic yielded 59.34 % TMP. Iron in Paleozoic is 1 % TMp'and increases during Alpine time to 19.67 % TMP and decreases during Middle and Upper Proterozoic to 6.81 % TMP. The chemical sediments genetic type is the most important, promoting 80.18 % TMP. The Palazu Mare deposit is oflarge size but its mineability is stiU problematic, due to hydrogeologic conditions and deep Iocation. The remaining depositsare of small and medium size.

Cu < 0.4 %. is in fact the class of porphyry copper assessed separately from other copper ore types due to low-grade and difficulties in mineability. They are assoCÎated with Banatitic and T ertiary magmatic subduction events and have small to medium size. They may be in economic terms due to the common presence

andlor Mo byproducts and association with epithermal ''''''r''' ...... '' < 15 %. This type of lower contents ore is no economic importance for the

time being. Iron occurs orthomagmatic ores with Ditrău alkaline massif yielding 92.43 % TMP. This is an intracontinentalrifting related setting during incipient evolution of the Alpine cycle in the Carpathian realm.

Besides major elements taken into account in the potential ilie metalliferous accumulations also contain several minor elements, among which at present

W, Se, Be, Sb are recovered directly the processing activity or indirect1y in the metallurgic process, in low amounts, whereas Co, In, TI, Co, can be recovered (especially in metallurgy), with values compatible wor1dwide (Niţulescu, 1962; Borcoş et al., 1983; Pandelescu et al., 1986).

One should also take into account ilie share of metallic elements possible to recovered from ilie tailings or old dumps, which generally cumulate considerable

volumes, important particularly for Ag, Pb, Zn and for the typical minor elements (Borcoş et al., 1978).

Metallogenetic: spec:ialisation of the main stages of geotec:tonic cydes/units and major geographic units

(Table 16)

quantiţative specialisation can inferred from variable association of the main mineralisation types (ferrous, non-ferrous and precious metals), from the value the ratio between ilie potentials (in of TMP) corresponding to the ferrous (iron + manganese) ores (lead + zinc + copper), as from the particular occurrence of some elements that determine the specific qualitative feature like W, V, Au,

Taking into account ilie geotectonic settings of the Alpine cycle, one can nhe,,,, ... ,,,'. an increase of the complexitY of the metallogenetic process, also noticed the variety the compositiooal of ore. This evolution line includes the n .. ''' .... ' .. " ..

ofthe value ofthe Fe+MnlPb+Zn+Cu from 65.78 in the rifting zone to 2.02 in the

Quantitative metallogenetic specialization tbe main of evolution

GEOTECTONIC COMMODITIES M E T A r:~ Pb+Zn Cu Au+~g Fe -

% % % %

PROTEtr'JI }Il Fe. Mn, Pb+Zn, Cu 0.70 0.08 0.02 86.44

CALEDONIAN Mn, Pb+Zn, Fe, Cu 21.29 9.60 0.02 2.1.19 HERCYNIAN- Fe, Mn, Pb+Zn, Fe<15%, Cu 1.64 0.07 0.001 92.58

UNCERTAIN PRE·41.PINE Fe,Mn 0.00 0.00 0.00 87.36

ALPINE Fe<15%, Fe, Pb+Zn, Cu<O.4% 7.98 1.88 0.02 35.40 Cu. Mn, Au+Ag ± Ti, V, Mo

-EXOGENOUS Fe, Mn, Fe<15% 0.00 0.00 0.00 91.27 ....................... ", Fe<15% Fe, Cu<O.4%, 9.11 2.15 0.03 26.87 -_ .. _--_ .. Cu. Mn, Au+Ag ± Ti, V, Mo

- Rifting Fe<15%, Fe. Pb+Zn, Cu, Mn 0.28 0.03 0.0001 4.24 - Spreading Cu 0.00 100.00 0.00 0.00 -Island are Pb+Zn, Cu, Mn 4.03 0.39 0.00 0.00 _ !!ita' .... · .Lion Fe, Pb+Zn, Cu<O.4%, Cu. Mn, Fe<1S%, Au+Ag 2-".29 5.05 0.06 57.31

- Banatites Fe, Pb+Zn. Cu Cu<O.4%, Mn 10.56 7.97 0.004 75.58 - Neogene Fe, Pb+Zn, Cu<04o/c, Cu, Mn. Fe<15%, Au+Ag 29.25 2.89 0.11 43.76

_ (':I"'m"';""'n Fe. Pb+Zn, Cu, Mn 1.84 1.41 0.004 95.71 ,.. Uneertain souree and position Fe, Au+Ag, Mn 15.91 0.00 0.03 77.43

L

Mn Cu<O;4%

% %

12.79 0.00 47.89 0.00

5.21 0.00 13.64 0.00

1.25 5.53

7.63 0.00 0.24 6.32

0.01 0.00 0.00 0.00 0.10 0.00 0.61 15.51 0.66· 5.12 0,41 23.22 1.02 0.00 6.63 0.00

S

Fe<15%

%

0.00 0.00

1

0.49 0.00

47.62

1.05 54.23

95.46 0.00

79.56 0.17 0.00 0.29 0.00 0.00

(XI IV

83

zones the island arc 6.59). The metallogenetic complexity the subduction stages is rendered evident by the increase of the contents of Au-Ag, and subordinately Mo-W-B, and

The ore composition of the Alpine cyc1es is relatively homogeneous, the differences consisting only the variation of the ratios between the associations of ferrous and non-ferrous ores; values this ratio were recorded in the Proterozoic cyc1es (190.61), and the lowest ones in the Caledonian cyc1e (5.29).

The geographic units that cumulate most of the potential are, as follows: South Dobrogea (155.36 miI. tons, exclusively iron), East Carpathians (1 mîl. tons - iron,

19aJlleS1e, lead-zinc, copper, the ferrous ores in amounts), South Carpathians (78.17 miI. tons iron, manganese, copper and lead-zinc, the ferrous ores prevailing), and Apuseni Mts 1.79 miI. tons - copper, iron, gold-silver,

with diversified mineralisations and locally with significant concentrations of gold-silver,copper and lead-zinc).

The economic aspects that include the activity (since ancient times) the value of the potential of mineable reserves and resources point out the importance of the geographic and/or geologic units. From this point of view it is to mention East Carpathians mainly to their and ores potential associated to the Neogene volcanism to Cambrian rhyoHtic one. The ........ , .... "'.'1""' .. ,,, .. of the Apuseni Mts consists especially in the volumes aud quality the gold-silver, lead-zinc ± and copper ores associated to Neogene volcanism and the ferrous, copper, ± ores related to the Banatitic magmatism. The westem part the South Carpathians (Banat and Poiana Ruscă) proved also to be important if one considers the iron accumulations associated to the Devonian sub-marine basic volcanism and to Banatitic magmatism, through porphyry copper and lead zinc ± and copper mineralisations related to the Banatitic magmatism.

to correlate qualitative interpretations of Umle-g,Oal;e ore formation with quantitative data for Romanian territory provides valuable information about metallogenetic specialisation, intensity of metallization and

of mineral deposits. The time-stratigraphic depositional sequences suggest the following

metallogenetic specialization various geotectonic cycles that is better expres sed as TMP:

Proterozoic cycle -Middle and Upper Proterozoic cycles - Mn, Cu, Pb,

Paleozoic - Mn, Fe , Cu, Pb, Zn (± Au, Cr, Ni, Th, U, REE); Upper Paleozoic cycle - Cu, Pb, (Mo, W, U, Th, Alpine cycle - Pb, Au, Ag, Mn, Mo Bi, Cd, Hg,

Ni, Th, TR). The paragenetic features the mineralisations point out the obvious tendency

metallogenetic specialisation that is rendered evident the ratio

84

which varies 1 the Proterozoic non-differentiated Caledonian cycle.

of metaHisation is preferentially related ta major magmatic events: LlU.U..., .... "'! vQlcanicity in granitoids during Upper

volcano-plutonic character in ~v~,,,,,,,,,v·,, of this kind yielded important skarn, porphyry

(very

(metamorphosed) that in the East Apuseni Mts. Their ec<mC'ml.C

' .... n' ... '" most of the accumulations are ,uuau··.ou,,",u the size of the ore being found at the lower !imit); medium-sized ore deposits are:

Ka:;~OaJre (Mn-Fe), Sebes Mts (Mn); Valley (Pb+Zn)', Bucătii Hill Gura Băii - Măcârlău Ivăscoaia - Novicior Muncel Ghezuri -Penigher Baia Sprie (Pb+Zn±Cu-Au-Ag), Băiut

Cavnic Suior Rosia Poieni (Cu), (CU±Au), Barza (Au), Montana (Au). World Au-Ag deposits at Montana ar Au, Ag .... vlf/v" .. '-' at Cavnic and Baia Sprie ~ .. ""t'Ti'." of the

the

Romania. classification of the to the size of

first places: Palazu (Fe), (Mn-Fe), Căpus

stresses out that

(Mn), Băisoara (Fe, Pb+Zn), (Fe), Ocna de Fier (Fe,

Teliuc -(Fe), Vatra one should

most of TMP is either non-mineable ar worked out. Quantitative and qualitative ch!lralcte.nSl:lllC)fi of the genetic types of mineralisations

the most types which most cases, .JLF>UU''' ......... v'"' (or hard ta be mined), of precipitation,

metamorphic formation (47.86 %), Dro,ces:ses (J j-h) (17.40 %), accumulations

ta metamorphosed corresponding non-differentiated cycles (carbonate, amphibolic and micaceous to the

graphite formations %), as well as to metamorphosed siliciclastic corresponding to the and

formations (PtzZ-3) (5.94 the genetic generated with a high mineability mention should of the

hydrothermal, skarn, porphyry and metamorphosed volcanogenic that yielded accumulations of lead-zinc, gold (silver) in the Alpine and the last

Caledonian cycle. Quantitative distribution ore regardless of the economic significance,

%) and manganese (9.53 %) ores are associated usually to the Proterozoic Paleozoic geologic representing 70 %. (4.36 %)

18 %) ores, are spread interval, starting up to the Neogene, the most productive geologic Alpine ones of the Miocene-Pliocene Tbe gold-silver ores (0.01 %) are mostly

a.o.,)V"" ....... ,y to the Neogene volcanism (87.30 %), constituting, with concentration and metallisation, the Metaliferi Mts.

85

The data obtained can contribute to the delimitation of the and which, by the geo-economic characteristic genetic models of the mineralization accumulations, discussion research programmes.

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silicioasa). C. Sare. Report, G.I.R. archives. -- , Simescu, St., Popescu, P., Gheorghe, R., Dita, A. (1990) Evaluarea potentialului de rezerve si

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OTHER CONSULTED DOCUMENTS

Metallogenetie maps, se. 1 :200,000 Metallogenetie maps, se. 1:50,000 ( ...... ,"'.,,:, .... rl for printing) Metallogenetic maps, second issue, se. 1:1,000,000 for printing) Map of the mineral resourees, se. 1:500,000 (prepared for printing) Structural, magma tic, metallogenetie map of the Metaliferi Mountains, se. 1 :200,000 Prognosis maps ofthe mineral resourees, se. 1:1,000,000; 1:500,000; 1:200,000 (unpublished)