24

TAE "GOLDEN QUADRANGLE" IN TBI i\IETAUFERJ MTS .. ROMANIA: WHAT DOES TAIS REALLY MEAl'i?

Gheorghe UDUBASA, Emili.n ROSU, Ioan SEGAEDI, Paul Mircea IVASCAN U Geological lnst itute of Romania, Caransebes SIreet 1. 78344 Bucharest

Abstract

The "Golden Quadrangle" of the Metaliferi Mts (GQMM) (sauthem pa" of Apusenl Mts.) belongs ta a large province of Miocene magmatism aod associated ore deposit~ developed in Slovakia. Hungary. Ukrai ne and Romania. Most of the calc-alkaline volcanic rocks in GQMM appear ta have been formed during a quite large time interval (14-7 4 Ma) However, the nearly synchronous magmatic activity in GQr..1M aod along Carpathian are2 evolved under difTerent geotectonic conditions. The GQMJvt is unique in thal it comprise~ both world-class gold deposits (Rosi a Montana) and rich ta very rich smaller depasit! showing an uncommon density of ore bodies an a km1 (e.g. Barza, Sacaramb). Additionally. the area is characterized by numerous (although many sub-economic) porphyry copper-gold deposits. as weB as by Au-Ag telluride ores, the richest so far known in Europe. The adakite­like tendency and most probably sulphur-undersaturated character of mOSI associated magmas, and their mineralizing fluids along with extensive fluid -rock interaction with ophiolitic basement are thought to have played a signiflcant role in the uncommon gold concentrat ion.

The Golden Quadrangle ofthe Metaliferi Mts (GQM1\'1). An Introduction

The GQMM, known also as the "Golden Triangle". "Golden Quadrilater", "Golden Quadrilateral", "das goldene Viereck" or "Patrulaterul Aurifer" is an unusual concentrat ion of gold or gold-bearing ore deposits related te Miocene magmatism. The GQ~1.tV1 covers an area of about 900 km1 and contain many historically significant mines, such as Rosia Montana; Frasin, Vuleoi - Corabia, Ruda Barza, Caraci - Tebea, Baita, Fericeaua, Almasul Mare, etc, known already from the Roman times (between 106-274 years. when Dacia was a province of the Roman Empire). During the last 2000 years the area was one of Europe's main goldfields. In 1941 it was appreciated that the GQMl\1 has produced approximately 1,000 tones of gold (Ghitulescu and Socolescu, 1941) and estimates afterwards might have doubled the figure. During the XV-th and XVllJ-th cemuries the gold production was of about 1,000 kglyear. According te Haiduc (1940) Ihe gold production of Romania (from which 60 te 70 % carne from the GQMM) shows an increasing trend from about 1,000 kg in 1924 te over 5,000 kg in 1937, then a decrease to about 2,200 kg in 1944. After the World \Var II the data became secret and nobody seems ta know and to reveal the real gold production in Romania. Anyhow, the total gold reserve ofthe ational Bank of Romania (over 100 t) comes mainly if nOi exclusively from domestic mines

Although most of the deposits in the GQMM are related not only genetically, but also spatially to the volcanic and subvolcanic bodies, there are a 101 of deposits hosted by the basement represemed either by older magmatic rocks ar sedimentary st rata. The faur pillars of the GQi\'1M are represented by Sacaramb, Zlatna, Baia de Aries and Caraci deposits, aII of them containing also Au-Ag tellurides (Fig. 1). The abundance oftellurides (Sacaramb) and the gold richness ofseveral deposits, e g. Barza, Valea Morii , etc I confer a peculiar feature of

o ## - Hydrothermal breccia pipe and velns occurrcnccs

Baia de Aries Area: OI - Valea Lacului, 02 - Aflllis

Rosia Montana - Bucium Area: 03 - Tarina, 04 - Celate, 05 - Cimic. 06 - Bucium-Rodu, 07 - Frasin, 08 - Contu, 09 - Corabia, 10 - Vulcoi

Zhltna Area: II-Izvorul Ampoiului, 12 - Viitori, 13 Babllia, J 4 - Brea7..3, 15 - Hanes, 16 - Metesan, 17 - Fata Baii, 18 - B..1ba, 19 - Almas - Dealu Negri~ 20 . Muncaceasca E, 21 - BorL.eSli

Hartagani - Sacaramb Area: 22 - Porcurea, 23 - Cord llrea, 24 - Piriullui Avram, 25 - Hondal, 26 - Coranda, 27 - Bocsa­Sacarunb, 28 - Sacanmb, 32· Omica

Bolcana Area: 29 - Traita, 30 - Baita Craciunesli, 31 - Trestia

BarLa Area: 33 - Hartagani , 34 - Ci inel , 35 - Bar/li E, 36 - Bara, 3? - Dealu Fetii

Tebca Area: 38 - Magura Tebei, 39 Carnei

Legend ~ Umlts of neogene volcanlc Pl"oduc 1s

D Necks and Shdlow Inlfuslve txx:Iles

Hydrothermal breccla pipes +/- velns:

• Sase melal+J· N..J. Ag o AJ..J, Ag +/- OO.se melol

Metasomatlc replacement: • Base melol

Hydrothermal Veln: • Sase mefal+/·Au,Ag velns O N..J,f'og+/- bose meTCI velns

• Hign - QJlphldation ep/thefmal I Cu, As )

• MerclJY occurences

• Au Ag tellurides occurences

F~, 1. Sketch wllh hydrolhermal ore deposlts In ao called 'GOLD QUADRAJlGLE', Soulh Apuseni M4s,Romanla. Occurences of Au Ag lellundes

o lOKm ""---===l

5

ROOaMaltgy~ /..- 04 ~zp

vv- Mures valle~ ~

~ - ---...... U'O<uHII' ~D • Deva "-_'.? 0'0

~ ~

26

GQMl\1, which is unique within the whole Miocene magmatic province of the Carpatho­mnoni3n area. Not only the high density of Ofe deposits, Î.e. the number of gold deposits on

. tm2, but also the relative overlapping of gold and copper (mainly porphyry type) deposits Îs

mer special feature of the GQMM (Fig 1). However, several large gold deposits, i.e . ..:aramb and Baia de Aries. are situated outside of porphyry copper area This fact is

fald meaningful: (1) the scurce of Au and Cu seems to be camman in mosI cases, but (2) gold might have 5upplementary source as well This is a new attempt to explain the uniqueness of the GQMM based on observed faca on new achieved data. Many detailed informatian can to be found in previous papers,

h as of Ghitulescu (1935), seemingly the first wha used the term "Quadrilatere Aurifere". tulescu and Socolescu (1935, 1941), lanovici et al (1969), etc

chemist ry and petrogenesis of magmatic roc ks

Following we are going to compare East Carpathians (EC) (Ukrainian Carpathians and -Gutai) and Apuseni Mountains (Ap) magmatic provinces, which evolved during the e time interval, between 14-7 Ma. Calc-alkaline magmas appear ta be generated in

~nse to different geatectonic context. In EC, clase to the front of accretionary prism of Carpathians, calc-alkaline magmas were generated as result of initial hydration of the enasphere during subduction slab-rollback and funher asthenospheric influx aII along the

~ch. directly related ta collisional processes (Seghedi et aL, 1998. in print . Kovacs, 1998. ublished thesis), whereas in Apuseni area situated cea 200 km far from the treneh, ealc­ine magmas appear ta have been generated in response te lithospheric extension

Balintoni and Vlad, 1998, Seghedi et al. 1998; Rosu et al., 2000a, this volume) The voJcanic rocks from EC show a continuum between basalts ta rhyolites, which ng ta ca1c-alkaline suite, in a rather narrow K20+Na20 ar K20 range. suggesting that

erentiation via fractional crystallization was a major process in generatian of these racks. ~ voJcanic rocks from Ap shaw a much narraw range. mostly andesites ta daCÎtes, falling

the caJc-alkaline field. but same crossing the boundary toward alkalic character (Figs. 2a. No abvious differentiation processes can be remarked (Rosu et al ., this volume). Another distinctive feature of the calc-alkaline magmas is that they have a rather low

HFSE abundances This is illustrated in the diagram NblLa-Ba/La (F ig. 3). in which NMORB md OlB plot on a steep array of variable NblLa, with relatively linie change in Ba/L.a. Subduction-related orogenic andesites and related caJc-alkaline products have much higher 3a/La. Higher BalLa suggest imponant implication of fluids in the magma generat ion, larger

the Apuseni rocks, as compared ta EC rocks. Some of EC magmas have higher NblLa iDWard om, which was interpreted as related to variable composition of asthenospheric "",rce (Seghedi et al., in print)

An important characteristic of Ap, as compared to EC is its higher Sr content and higher - N ratia for large a pan of the samples (Figs. 4 and 5). This specific geochemical behaviar .:omprises part of the Apuseni Mountains calc-alkaline magmatic rocks in a particular association. i.e. the adakite of Defanl and Dmmmond (1990). The adakile \Vas defined as an

ermediate te acid calc-alkaline volcanic or hypabyssal rock characterized by high AhOJ, r and low Y and heavy REE, MORB-like Sr and Nd isotopic signature The adakite genesis.

1CC0rding to Defant and Drummond (1990) and Martin (1999) suggest denvation rrom high­pressure partial melting of subducted oceanic crust or underplated basic material Tbieblemont et al. ( 1997), based on the study of major mining areas (\Vestern USA, Chile, Papua New Guinea) suggests that mineralization (epithermal and porphyry) preferentially concentrates in adakite-l ike rocks. As can be seen in Figs. 4,5 the Apuseni Mountains

27

adakite·like rocks. show higher Y content. even they host important porphyry and epitherm deposits. oolY'p'3rtially overlap the mÎneralized field contoured by Thieblemont el aL, (1997

The 87Srr'Sr ratia generally Încreases with increasing Si01 in the Ee rocks (Fig. t which was attributed ta combined crustal contaminat ion and fractianal crystallizatÎ( (Seghedi et al , in print; Kovacs, 1998, unpublished thesis) In the Apuseni province high 87Srf6Sr belongs ta older rocks (> 13 Ma), whereas younger ones show lawer values (Rosu al., thi s volume). This kind of behavior preclude contamination and fractieoa! crystallizati(

5 i ! i I i i I I I

4 ~ Ee 3 i-

K.O

2 r Medlum-

1 ~.

Low-K O ' 50 55 60 65 70 75 80

a, SiO,

16

14

12

10

N~O+I~,o 8 - ---Ee 6

Rhyol~ 4 /f --r .' • as' s 2 '--- Bareltic Basa~ an esite

I O 35 40 45 50 55 60 65 70 75 80

b, SiO.

Fig. 2 KD, s. SiQ diagrarn in Apuseni (Ap) and East Ca'l'athians (EC) magma!ie rocks (a) Total alkali \ S. SiQdia2ram (TAS) in Aouscni fAD) and East Caro..1.thians (EC) malZmatic rocks I

processes and suggest that the most impo"ant process involved in the generation of Apus.

28

~.." .. is a variable degree of partial melting of a isotopically depleted source, but rather ',.,=..., in incompatible elements (Rosu el aL, this volume, Seghedi el al. , in preparation). J""Nd/loNd ratia shows lawer values for Ee as compared ta Ap and 00 obvious

I~=_ with increasing SiO, (FiS 7). 2.0,----------------,

1.5

Nb/Lal.0

0.5

10

CXl O

20 30 40 50 Ba/la

Fig. 3. NblBa VS. BaILa <hagram for Apuseni (Ap) and East Carpathians (EC) Neogcne m::uunatic provinces. MORS and 018 aftcr Sun & McDonou~h

The Ee rocks have been atuibuted 10 derivat ion from scurce regions within the mantie sphere thal had been previously enriched by subduction-related processes and further

high level magma chambers experieocing crustal contamination and fractiana! -saIization (Seghedi el al. in print, in preparat ion). Different conclusions were reached for

rocks which show a transition from normal calc-alkaline to alkaline adakite-like magmas,

150 I

~ P

100 r daklt&-llk.

SrlY

~ r Ee o t

Nonne' ..... . -. .... _ .... -'-'. , .. __ '1_' u "

___ i_. _

48 52 56 60 B4 68 72 76 Slo..

Fig. 4. SrN liS. Si? diagram for Apuseni (Ap) and East Carpathians (Eq

mall;matic provinccs ~10RB and OIB after Sun & McDonou,Rh.(1 989).

29

120 Ada!<f1a fteld ~

&N eo ~ A i ,-l

40

O L--~ ~~~ ° 10 20 ~ 40

Fig. 5. SrN \'5 . Y for Apuseni (Ap)~d Eas1 Carpathians (EC) Neogene magntatic provinces. Adakitic field from Defant and Drummond (1990) and Thieblemont el al ., (1997) and mineralized field charactcristic for adakite-like magmatism rrom Thieblemont el al ., (1997)

0,711 ~ 0,709 [

"'gh r 0,707 ~

0,705 l

OIB

0,703 ORB

...... , EC

J J J

. J ,,' I

J

~ ~ M ~ ~ ~ ro A n SIC,

Fig, 6,"SrT Sr VS, Siq for Apuseni (A p) and East Carpalhians (EC) Neogene magmatic provinces. MORS and 0[8 after Sun & McDonough, (1989) .

0,5131 I ' ."",. , -, 0.5129

I OI.

'~dI"Nd 0.5127

0,5125 EC

0,5123 ~ ~ M ~ 62 ~ 70 74 78

SIO, Fig. tU NdI'""Nd vs . SiO for Apuseni (Ap) and East Carpathians (EC) Nco'lcnc ma.v.matic provinces. MORB and 018 after Sun & McDonou'lh. (1989) .

30

UI significant contamination and fractional crystallization. rather characteristic for rapid t of magmas in the extensional regime in which the Apuseni magmatic province

ved The source region is heterogeneous. and high L[LE contenl are in a favar of a source h was enriched by subduction processes, in an old tectonic event, or/and during the

goeene-Miocene times subduction. prior to initiation of rollback processes (Rosu el al., volume, Seghedi el al , in preparation).

erai Deposits - The Facls

The GQMt.\i1 comprise a large number of deposits either word-class, e.g. Rosia lana, Barza or smal1. very rich gold deposits developed on quite restricted areas, e.g.

:...III2f3mb, Caraci, etc. Various types of deposits are known in the area (1) gold ore veins. common (e.8 Barza), (2) Au-Ag-Te ore veins, very characlenstic (Sacaramb): (3)

hyry-copper sold, typically developed, e.8. Bucium-Tamiia, Bolcana-Troila, Valea 'i, Voia; (4) Au-base melal breccia struclures (breccia pipes) (es Baia de Aries), Au minated in sedimentary rocks, accidental (Coranda-Hondol, Larga), (5) Au disseminated

altered magmatic rocks. rare (Rosia Montana). (6) Au-base metal Ofe veins. less cammen "'rroita, Muncaceasca).

The gold veins are localized in various environments. The majority (disseminated included) oecurs in magmatic rocks, either subvolcanic stocks or lava flaws. The

ment of the gold veins hosting volcanic structures is maioly represented by Mesozoic d arc-ophiolites. as a part of the Main Tethysian Suture (Sandulescu, 1984), with

~ fleant aod subordinate participation of Mesozoic sedimentary rocks and metamorphic =-rmations, respectively. In some cases, ophiolites of Mesozoic age form lhe hOSl of lhe gold

S, egal Baila-Craeiunesli. Rarely there are gold veins in sedimenlary rocks, e.g. al ~ericelii Hill, Zialna area FUr1her delails can be found in Ihe papers of Ghilulescu (1935),

!ulescu and Socolescu (1941), Borcos el al ., (1984), Udubasa el al. (1992). The gold fineness is generally high, except the ores containing Ag sulphosalts (e.g. Rosia

nlana) A very typical geochemical feature of many gold ores is the Au-Te-Mn triad, a eralogical expression of Au(Ag) tellurides being associated with rhodochrosite and

ndite (Sacaramb, Caraei, Baia de Aries, etc). The vertical development of the veins is erally limited, but sometimes ample, reaching as much as 600m (e.g. Sacaramb). There

ft as a rule short veins, but highly concentrated on small areas (eg Sacaramb: 230 :anslkm2

) Vein lengths over 1 krn are rare, e.g. the Arama vein al Bucium, in fact a Cu-Au vein. An interesting remark has been made by Bostinescu (1984) regarding Ihe dominant

als of the porphyry systems in the Metaliferi Mountains (roughly coincident to the GQMM), i.e. Cu-Au in the internal porphyries, for bodies emplaced in ophiolitic basement al Cu-Mo in the peripheral porphyries. for bodies intruding metamorphic basement (e.g.

sia Poieni, Deva).

'lineral Deposits - The Interpretat ion

is here proposed that the gold richness of the GQ~1M is due to ' 1) the normal to adakite-like calc-alkaline magma sources; ~) the "processing" of the ophiolitic basement, as a supplementary scurce of Au and Cu

and ofsedimentary formations, as a supplementary source ofM_n and Te Two Iypes ofarguments either indirect or direct can be presented in favor ofthe item (2).

31

Indirect arguments: Comparing with the Baia Mare area, with dominant Pb-Zn-Cu eres and subordinate Au-Ag, the GQMM has an ophiolitic basement, as a feliel ofthe Main Tethysian Suture and a the evolutian toward adakitic-like character of the magmas; the Baia Mare area have in ilS basement only a very thin pile of ophiolitic rocks from the Pienniny Klippen and the adakite-like tendency is lacking.

Direct arguments' Locatian of same gold ores within ophiolites (Baita-Craciunesti) and occurrence of Au-AS tellurides as local pods exclusively within altered ophiolites (Coranda-Hondol, that is a Zn-Pb-Au ore). In addition, abundant rutile development, e.g. in the Barza (Caljlen) gold deposit (Udubasa, 1978) may also suggest mobilizat ion of Ti from the Fe-Ti ores Of minerals commonly found in the ophiolites.

lsotope data give further argumellts: The sulfur isotope in the sulfides and some sulphates of the GQMM is around zero &]4SO/00, but deviations are known (Udubasa and Gaftoi. 1985; A1derton and Fallick, 2000; Rosu et al., 2000b). In many cases the lack of isotopic equilibrium is obvious, induced both by vein shearing (Bolcana-Troita, vein cutting aeross the porphyry Cu-Mo-Au ores) or by fluid mixing. whieh resulted either in a modified isotopes fraetionation (Magura Tebei) ar even in an inverse fractionation (Sacaramb) (Udubasa and Gaftoi. 1985). The poljlhyry copper ores show a gradual change of B"S values from O to 2%0 in the "marginal", Mo-rich porphyries to O to J11'00 in the "internal", Au rieh porphyries (Borcos and Gaftoi, 1985). The sulfur in the fluids could be interpreated as belonging te a magmatie souree which interaet speeifieally with basement sedimentary or magmatic formations (Udubasa and Gaftoi, 1985; Aldenon and Fallick, 2000; Rosu el al .• 2000b).

Oxygen and hydrogen isotope analyses are only few from the Saearamb-Magura area (Alderton and Fallick, 2000). Escape of several plotting poin!s rrom the primary magmatic water box might have been eaused either by fluid boii ing or by fluid mixing. There are stiH scarce data to conci ude convineingly about the true nature of the tluids. Investigation of Sr isotopes of altered rocks in the same area (Aldenon el al ., 1998) suggest a metasedimentary signature, with Sr being leached out from the underlying strata.

Th e geoc/,emical triat! Au-Te-/Wn is another eharacteristic of many gold eres in the GQivf.M. AII the elements seern te have been supplemented to the dominant magmatic tluids by the underlying ophiolites (Au) assoCÎated with sedimentary Mn ores. Beaty and Manuel (1973) depieted highest eontents of Te in lirnestones and shales (abundantly developed within the GQMM), i.e. of 1,000 to 1,700 ppb and 800 ppb, respectively. Afifi et al., (1988 concluded that the source of Te in the Au-Ag telluride ores might be ofmagmatic origin and "the reasons for enrichment of some system with tellurium are open to speeulations" (p.402). Age determinations of tellurium (Srinivasan et al. , 1972) complicate once more the thing related 10 the telluride eres from the GQMM. An ere sample from Fata Baii, Zlatna area (type locality ofnative tellurium) gave an age of 33.9 ±8.4 Ma by using the IJOTe_I 30Xe ratie. Thi is outside ofage interval efthe whole Miocene magmatism (14.7-7.4 Ma) in the Metaliferi Mts. (Roşu et al. , 1997).

Conclusions

(1) Normal calc-alkaline te alkaline adakite-like magmas in the Ap are essential for or forming proeesses due to their high fluid eentent. Mineralizing fluids along wit extensive fluid-rock interaetion with basement are thought ta have played a significan role in the uncommon gold concentrat ion.

32

The basement of the GQ~1M cannot be regarded as a passive counterpart of the magmatic and postmagmatic events. In the Ap the basement is heterogeneaus and includes al50 the magmatic products of the Main T ethysian Suture of Mesazoic ase. ~1elamorphic rocks and various sedimentary formations are present and they were repeatedly affected by deformations and fracturing The involvement of the ophiolitic basement in the metal enrichment of Miocene Dfes may suggest thal it could represent a 5upplementary SQurce ar secondary input of gold and copper

The comparison with Baia Mare area (Oas-Gutai Mts.), where the magmatism ofthe same age are largely developed and where Pb-Zn-Cu ± Au-Ag Dfes prevail and no ophiolitic basement seems ta be involved, shows that the conclusion (2) might be somewhat carrect. This fact adds to the differences in the geotectonic conditions of the (wo areas, i.e. Ee and Ap, whieh were more favoring in the Ap for gold mineralizations ta occur.

The heat engine of the smal! andesitic stocks in the GQMM is seemingly not sufficient ta circulate big amounts of fluids necessary ta produce such rieh deposits. A1derton and Fallick (2000) accepted the hypothesis of Szafian et al (1997) conceming a gravity model for a "pluton" extending down ta 10 km in Apuseni area However, new gravimetric data (L. Besutiu, personal communication) does not suppon such a hypothesis. Smal! maximum oecurs only in the Zlatna zone and the rest of the area lies rather in a gravity minimum. On the other hand, rather low volume of hydrothermal fluids in GQMM (suggested by inconspicuous alterat ion halos) do net require larger plutons for maintain heat scurce, as the magmas are generated al high temperarure (see the adakite-like tendency) and had a rather rapid ascent and short-time residence in crustal magma chambers (see the lack of obvious rraetional crystallization) in the inferred extensional tectonic setting (Balintoni and Vlad, 1998: Seghedi et al ., 1998; Rosu et al. , 2000a, this volume)

In the MetaJiferi Mts several magmatic events succeeded and spatially overlapped in the IaSI 140 million years, i e ophiolites (-140 Ma), Lower Cretaceous (- 80 Ma) granitoids, Upper-Cretaceous - Lower PaJeogene - calc-alkaline banatites (-60 Ma) and calc-alkaline Neogene rocks (14.7-74 Ma), and finally a later smal! volume magmatic evenlS producing shoshonitic roeks (1.6 Ma) (Ianovici et al. , 1969; Pecskay et al., 1995, Rosu et al. , 1997). Eaeh e\'ent was followed by fluid circulation of difTerent extent. Therefore, in the IaSI 140 miII ion years the GQMM was repeatedly heated and cooled, circulated by fluids of different composition and temperature, a fact which increased the emhropy of the whole sYSIem, which probably was brought "at the edge of chaos" (Yu, 1999), a prerequisite of large ore deposits ta occur.

The conclusion (5) give emphasis to the ore potential ofthe Neogene magmas itself There are many data showing an early partition of copper and gold in the residual volatile rich phases in the porphyry copper ores (Pintea, 1996, unpublished thesis, this volume, Ivascanu et al. , this volume), a faCI experimentally proved b)' Simon et al (2000)

Wyborn and Sun (1994) suggested the magma source-rock for the formation of high­gold deposits is sulphur-undersaturated. The removal of sulphur can be a result of succesive extraction in the lithosphere of sulphur-saturated basaltic melts in successive evems (which would left behind a small amount of sulphide and highly enriched gold and copper) in the same realm, which is the case history of GQMM See the conclusion (5 ) .

33

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