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Caves Formed Within Upper Cretaceous Skarns at Bˇait

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Caves Formed Within Upper Cretaceous Skarns at Bˇait 1693 The Canadian Mineralogist Vol. 40, pp. 1693-1703 (2002) CAVES FORMED WITHIN UPPER CRETACEOUS SKARNS AT BAITˇ ¸A, BIHOR COUNTY, ROMANIA: MINERAL DEPOSITION AND SPELEOGENESIS BOGDAN P. ONAC§ Department of Mineralogy, University of Cluj and Institute of Speleology “Emil Racovit¸ˇa”, Clinicilor 5, 3400 Cluj, Romania ABSTRACT The Bˇait¸a metallogenic district, in Bihor County, Romania, is genetically connected to a deep-seated Upper Cretaceous granitic pluton. Within this district, several bodies of skarn host economic concentrations of Mo, W, Bi, Cu, Pb, Zn, B, wollastonite, and marble. During mining, numerous karst cavities were encountered. Minerals such as wittichenite, antimonian luzonite, natrolite, quartz, chalcanthite, rosasite, glaukosphaerite, aurichalcite, azurite, malachite, norsethite and, more commonly, calcite, aragonite, hydromagnesite, and goethite were found within these skarn-hosted caves as crusts, coralloids, minute crystals, aggregates, and earthy masses. Some of the minerals are of hydrothermal origin, whereas others are interpreted to have formed during episodes of hydrothermal or vadose alteration. A third group consists of minerals that were precipitated from low- temperature karstic waters. Although most skarn-hosted cavities exhibit the classical features of meteoric-water-induced cave, their mineralization, morphology, and position within the skarn support a hydrothermal or a mixed hydrothermal-vadose origin. Keywords: skarn, hydrothermal karst, cave, mineralogy, speleogenesis, Bˇait¸a, Bihor County, Romania. SOMMAIRE Le district métallogénique de Bˇait¸a, comté de Bihor, en Roumanie, est génétiquement associé à un pluton crétacé supérieur profond de composition granitique. Dans ce district, plusieurs masses de skarn contiennent des concentrations économiques de Mo, W, Bi, Cu, Pb, Zn, B, wollastonite, et marbre. Au cours de l’activité minière, de nombreuses cavités karstiques y ont été trouvées. La présence de minéraux tels que wittichénite, luzonite stibifère, natrolite, quartz, chalcanthite, rosasite, glaukosphaerite, aurichalcite, azurite, malachite, norséthite et, plus couramment, calcite, aragonite, hydromagnésite et goethite, a été notée dans les grottes développées à l’intérieur des skarns. Ces minéraux se présentent sous forme de croûtes, de coralloïdes, de petits cristaux et d’aggrégats. Un sous-groupe de ces minéraux a une origine hydrothermale ou vadose. Par contre, les minéraux d’un troisième groupe ont été précipité à partir des eaux karstiques à basse température. Bien que la plupart des cavités des skarns montrent des traits classiques d’une grotte due à des eaux météoriques, leur minéralisation, leur morphologie et leur position à l’intérieur des massifs skarnifiés étayent une origine hydrothermale ou hydrothermale-vadose. Mots-clés: skarns, karst hydrothermal, grottes, minéralogie, spéléogenèse, Bˇait¸a, comté de Bihor, Roumanie. INTRODUCTION such cases, economic ore deposits, mainly of Pb–Zn, may be associated with the host rock (Mozgova 1963, Hypogene caves are formed by dissolution by deep Dz˙ul/y´nski & Sass-Gustkiewicz 1989, Sass-Gustkiewicz / CO2- or H2S-enriched hot fluids as they approach the & Dz˙uly´nski 1998). This type of hydrothermal cave has surface (Egemeier 1981, Palmer 1991, Ford 1995). Such received much less attention than the classical dissolu- caves develop at the expense of sedimentary or meta- tion-induced cave. morphic carbonate rocks. According to Ford & Will- Several Romanian caves show evidence of hydro- iams (1989), caves referred to as “hydrothermal” thermal mineralization (Nedopaca & Grama 1987, Onac develop when hot fluids rise through pores or along fis- et al. 1995); however, only a few were documented to sures, faults, brecciated zones or bedding planes and be dissolved or mineralized by postmagmatic solutions cool in carbonate rocks with or without mixing with (Mârza & Silvestru 1988, Mârza et al. 1995, Ghergari shallow meteoric waters. As discussed in this paper, a et al. 1997, Damm 2000, Onac et al. 1995, 2000). particular type of hydrothermal cave occurs where In this paper, I focus on the origin of the minerals volcanogenic fluids trigger the dissolution process. In found within the skarn-hosted caves at Bˇait¸a, in Bihor § E-mail address: [email protected] 1693 40#6-déc-02-2443-13 1693 1/3/03, 15:35 1694 THE CANADIAN MINERALOGIST County. Knowledge of their mineralogy may help to the metamorphosed Triassic carbonate rocks of the answer the question of whether hypogene or supergene Vetre Nappe are in tectonic contact with quartzite and processes triggered the mineral deposition, which would hornfels belonging to the Cos¸uri Beds (Vˇalani Nappe) provide an interpretation of the speleogenesis of these (Matyas¸i et al. 2001). The Aries¸eni Nappe covers the cavities. Vetre unit unit and consists of Permo-Triassic detrital rocks (Fig. 1). GEOLOGICAL SETTING Intrusive rocks are represented by Upper Cretaceous (Balintoni 2001) (Alpine) calc-alkaline granitic rocks The Bˇait¸a metallogenic district is located in the west- (“banatites”: Codarcea 1931). The skarn-type mineral- ern part of the Bihor Mountains, in the upper reaches of ization consists of economic concentrations of Mo, Bi, the Cris¸ul Bˇait¸ei River (Fig. 1, inset). Old mining docu- W, Pb, Zn, Cu, B ± Au, Ag, Te, and Fe. The rich mag- ments provide evidence of continuous mining activity nesian and calcic skarns of Bˇait¸a and their associated from the Middle Ages up to the present (Stoici 1983). ore deposits are connected to a deep-seated pluton of More than 100 mineral species have been identified in granitic to dioritic composition. Several dykes, ranging the skarn deposits of the district. Hemimorphite, kotoite, in composition from rhyolite to basalt, are related to the makovickyite, padˇeraite, and szaibelyite have their type Cu–Pb–W–Bi–B ores (Stoici 1983). The ore deposits localities in the district (Udubas¸a et al. 1992, Udubas¸a occur as metasomatic columns or irregular bodies and 1999). impregnations in marbles. The geology of the deposits The major structural units of the region are the Bihor was the subject of many detailed studies, carried out Unit, in para-autochthonous position, consisting of Up- among others by Stoicovici & Stoici (1972), Cioflica et per Jurassic and Lower Cretaceous limestones, and the al. (1974, 1977, 1995), Cioflica & Vlad (1979), Stoici Apusenides (Balintoni 2001). The latter include the (1983), and Matyas¸i et al. (2001). Codru and Biharia Nappe systems, represented in the area by the Vetre and Aries¸eni nappes, respectively DESCRIPTION OF CAVES IN SKARNS (Bordea et al. 1975). The Vetre Nappe is the lowermost unit of the Codru Nappe system in the Cris¸ul Bˇait¸ei re- Most of the cavities discussed here were intercepted gion and comprises a complete Triassic sequence. The by mine adits and shafts. As listed in Table 1 and shown assemblage consists of quartzite and hornfels (Ladinian in Figure 1, two mining sectors contain these caves, to Lower Carnian), the Frˇasinel dolomite marble Cos¸uri and Frˇasinel–Antoniu. The most important cat- (Carnian), and the Bˇait¸a marble (Norian) (Bleahu et al. egory concerns caves developed within the skarns (the 1994). Within the upper part of the Cris¸ul Bˇait¸ei area, main subject of this paper), but also included are classi- FIG. 1. Simplified geological map of the Bˇait¸a metallogenic district, in Bihor County, Romania, showing the location of the mining galleries in which the caves were intercepted. 1: Aries¸eni Nappe, 2: Codru Nappe, 3: Bihor Unit, 4: Geological boundaries, 5: Fault, 6: Thrust fault, 7: Adits, and 8: Shaft (modified from Stoici 1983). 1693 40#6-déc-02-2443-13 1694 1/3/03, 15:35 MINERAL DEPOSITION IN CAVES FORMED WITHIN SKARNS, ROMANIA 1695 cal dissolution-induced caves. The size of the caves tron-microprobe analyses (EMPA), atomic absorption varies between 8 and 550 m in length. The cavities con- spectrometry (AAS), infrared spectrometry (IR), as well sist of medium-size passageways (or rooms), from as carbon and oxygen stable isotope analyses. Textural which small irregular side passages may develop. The and morphological observations were undertaken using cave walls are lined with thick crusts of calcite and dis- both optical microscopy. X-ray data were obtained by play exotic minerals. No other dissolution or erosion means of Philips PW1800 and DRON–3 diffracto- features are present in these caves, except for some cu- meters. Operating conditions were 45 kV at 40 mA and polas and corrosion notches located in the ceiling of the 20 kV at 20 mA, respectively, using CuK␣ radiation, caves. The most common speleothems found in the and quartz as internal standard. All samples were con- skarn-hosted caves are coatings, coralloids, crusts, flow- tinuously scanned from 6 to 70° 2␪ with a step size of stones, moonmilk, powder, minute crystals and, less 0.025° 2␪. The characterization of the mineral species commonly, stalactites and stalagmites. This morphol- relied solely on the XRD patterns in cases where the ogy and mineralogy are indicative of cavities whose spectrum was complete and well resolved. In this case, origins where either partially or completely hydrother- unit-cell parameters for the analyzed minerals were also mal in nature (Ford & Williams 1989). calculated. Where the spectra obtained showed evidence The host rock of the investigated caves is represented of multiple phases, additional investigations (i.e., EDS, by either calcic (Cos¸uri sector) or magnesian and cal- EMPA, AAS, IR and, where possible, thin section ob- cic-magnesian skarn bodies (Frˇasinel–Antoniu sector). servations) were made. These skarns formed at the expense of Mesozoic car- A JEOL JXA–8600 Superprobe (Department of bonate paleosome belonging to the Codru Nappe sys- Earth Sciences, University of Bristol) was used in the tem (Stoici 1983). On the basis of their spatial wavelength-dispersion mode, under the following con- development, the caves closely follow the metasomatic ditions: excitation voltage 20 kV, specimen current contact between Cos¸uri Beds and the skarn bodies. Since 5 nA, peak count-time 20 s, background count-time 10 this contact is inclined at about 45–70°, the caves show s.
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