ReOs molybdenite and LAICPMSMC UPb zircon geochronology for the Milpillas porphyry copper deposit: insights for the timing of mineralization in the Cananea District, Sonora, Mexico
Geocronología de ReOs en molibdenita y LAICPMSMC UPb en circón para el pórfido cuprífero de Milpillas: aportaciones para esclarecer la evolución temporal de la mineralización en el Distrito de Cananea, Sonora, México
Victor A. Valencia1,*, Benito NoguezAlcántara2,3, Fernando Barra1,4, Joaquín Ruiz1, George Gehrels1, Francisco Quintanar2, and Martín ValenciaMoreno3
1 Department of Geosciences, University of Arizona, GouldSimpson Building 1040 East Fourth St., Tucson, Arizona 857210077.
2 Servicios Industriales Peñoles, Blvd. Navarrete 2778, 83200, Hermosillo, Sonora.
3 Estación Regional del Noroeste, Instituto de Geología, Universidad Nacional Autónoma de México, Apartado Postal 1039, 83000 Hermosillo Sonora, México.
4 Instituto de Geología Económica Aplicada, Universidad de Concepción, Chile. * firstname.lastname@example.org
Manuscript received: January 20, 2005
Corrected manuscript received: October 11, 2005
Manuscript accepted: October 26, 2005
New geochronological data presented here improves the understanding of the temporal evolution of the Cananea Mining District, and particularly of the Milpillas porphyry copper deposit (northeastern Sonora, Mexico). Uraniumlead zircon analyses, using laser ablation ICPMS multicollector, from the quartz monzonite porphyry unit that host the mineralization at the Milpillas deposit, yielded a crystallization age of 63.9 ± 1.3 Ma (2sigma). ReOs molybdenite ages from two drill core samples from more than 500 m depth yielded an identical age of 63.1 ±0.4 Ma (2sigma), suggesting a restricted period of mineralization. These ages indicate that the Milpillas deposit is the oldest Laramide porphyry copper deposit recognized so far in the Cananea District.
Our new ReOs data in addition to previous ReOs data, suggest that mineralization within the district, occurred within a 4 m.y. period in three discrete pulses at 59 Ma, 61 Ma and 63 Ma. This is in contrast to the previous model in which mineralization at the Cananea District was the result of a continuous hydrothermal system that started at 62 Ma and ended at 52 Ma.
The first attempt to determine the timing of mineralization and magmatism of Mexican porphyry copper deposits (PCDs) was by Damon et al. (1983). Later, McCandless and Ruiz (1993) provided the first ReOs molybdenite ages for PCDs in the US Southwest and northern Sonora, Mexico, and concluded that there were two periods of regional mineralization, at 7470 Ma and at 6055 Ma. More recently, Barra et al, (in press) provided new ReOs molybdenite ages for ten porphyry copper deposits from northern Mexico. Their data expands the Laramide mineralization event to 50 Ma, and suggests the idea that porphyry mineralization could also have occurred at 64 Ma. The older period of mineralization (7470 Ma) has not yet been recognized in Mexico.
In recent years, and with the advancement of geochronological analytical techniques, new studies have been performed in order to determine the timing of mineralization and the duration of hydrothermal systems in different porphyry copper provinces of the world, particularly in the Chilean province (Marsh et al., 1997; Ossandoneet al.., 2001; Bertens et al, 2003, PadillaGarza, 2003; Masterman et al, 2004; Maksaev et al, 2004). In the North American Southwest porphyry copper province advances have been made in only a few deposits (i.e., Sierrita, Jensen, 1998; Herrmann, 2001; Morenci, Enders, 2000; Bagdad, Barra et al, 2003; La Caridad, Valencia et al, 2005). However, at the district level the timing of the different deposits is generally not well constrained (i.e., Cananea District in Sonora, Mexico and Pima District in Arizona, USA).
The Cananea District, located in northeast Sonora, Mexico (Figure 1), has produced more than 3.5 million tons of copper (PérezSegura, 2001; written communication). This district is characterized by a cluster of deposits that includes the world class porphyry copper deposit of Cananea, Lucy and Maria mines, Milpillas and Mariquita projects and Los Alisos, El Toro, El Alacrán and La Piedra prospects (Figure 2). These deposits have reserves of over 11 million tons of copper (Long, 1995).
In spite of the economic importance of the Cananea District, limited geochronological work has been done on the timing of mineralization and magmatism (Anderson and Silver, 1977; Damon et al, 1983; McCandless and Ruiz, 1993; Wodzicki, 1995; CarreónPallares, 2002). An important remaining question is whether the multiple centers of mineralization in the district are the result of one episode or multiple shortlived episodes.
In this paper, we report data from the Milpillas deposit, which is the prime example of a hidden deposit in Mexico, and specifically in the Cananea porphyry copper district, which ranks among the three largest known porphyry copper districts in North America. Here we use UPb in zircons and ReOs in molybdenite to constrain the timing of magmatism and molybdenite mineralization in the Milpillas deposit. We also compare the new data with previous ReOs molybdenite ages from ore deposits in the same district (McCandless and Ruiz, 1993; Barra et al, in press). The question of the number of mineralization episodes in the district is relevant both to the metallogeny of the Southwest North America and to provide guidelines for the development of exploration programs.
REGIONAL GEOLOGICAL SETTING
The Cananea District lies on the southwestern edge of the North American craton (Campa and Coney, 1983; Sedlockeet al.., 1993) (Figure 1). The basement of the terrane is the PrecambrianPinal Schist (1.68 Ga), intruded by 1.41 1.48 Ga anorogenic granites (Silver et al, 1977; Anderson and Silver, 1981; Anderson and Bender, 1989). Paleozoic sedimentary rocks in Northeast Sonora (GonzálezLeón, 1986; Stewart et al, 1990; Gehrels and Stewart, 1998; Blodgett et al., 2002) represent the southern extension of the Cordilleran miogeocline and platform sequences (Rangin, 1978; Campa and Coney, 1983; Stewart, 1988) and these rocks are represented in the district by the Bolsa (Cambrian), Abrigo (Cambrian), Martin (Devonian) and Escabrosa (Mississippian) Formations, and part of the Permian Naco Group (Meinert, 1982; Wodzicki, 1995, 2001).
Precambrian and Paleozoic rocks are overlain by TriassicJurassic volcanic rocks (in the Cananea District are the Elenita and Henrietta Formations; Valentine, 1936), which are intruded by Jurassic plutonic rocks. These rocks are part of a continental magmatic arc that extends from California, USA to Durango, Mexico (Anderson and Silver, 1978; Tosdal et al., 1989; Jones et al., 1995). The Bisbee Group of Late JurassicEarly Cretaceous age crops out northeast of the area, but it is absent in the Cananea region, suggesting that this area was a topographic high during the Mesozoic (McKee and Anderson, 1998). Plutonic and volcanic rocks of Late CretaceousEocene age are widespread throughout southern Arizona, New Mexico and northern Sonora and were emplaced during the Laramide orogeny. Most of the porphyry copper deposits in southwest North America are associated with the Laramide orogeny (7550 Ma, Shafiqullaheet al.., 1980). The geologic setting of these deposits has been discussed in detail by Titley (1981,1982), Titley and Beane (1981), Titley and Anthony (1989), and Titley (2001).
After a period of quiescence of about 20 m.y., caused by the westward migration of the magmatic arc (Coney and Reynolds, 1977; Damon et al., 1981; Damon et al., 1983), intensive magmatism occurred and is represented by extensive volcanic sequences of Oligocene age (3025 Ma)(Shafiqullahe et al. , 1980; Damon et al., 1981; RoldanQuintana, 1981). During the Miocene, midcrustal extension and corecomplex formation occurred in Sonora between 2712 Ma (Gans, 1997) causing disruption and rotation of the Cananea District (CarreónPallares, 2002).
Numerous authors have described the geology of the Cananea District since the early 20th century ( i.e. , Emmons, 1910; Valentine, 1936). More recently, studies have focused on the geology of individual deposits that form part of the district (i.e., Perry, 1961; OchoaLandin and Echavarri, 1978; Meinert, 1982; Bushnell, 1988; Wodzicki, 1995; 2001; CarreónPallares 2002). de la Garza et al. (2003) performed the first descriptive work on Milpillas. This ore deposit is located in a zone of extension, common in the Basin and Range province, which is referred as the Cuitaca Graben (Figure 2).
The Milpillas deposit located in the northern part of the Cananea District, is included within the downdropped block 7 km wide Cuitaca Graben, which cuts the Cananea region from north to south (Figure 2). The eastern portion of the graben is at a shallower level than the western portion and is dominated by Tertiary gravels, Quaternary alluvium, and erratic outcrops of Laramide volcanic units. The deeper western part of the Cuitaca Graben is dominated by Quaternary alluvium. Close to the eastern boundary of the Cuitaca Graben, a small horst is present where scarce altered and oxidized outcropping reveals the existence of the Milpillas ore deposit (Figure 2).
The oldest rock unit that crops out in the Cananea District is the Precambrian Cananea Granite (Figure 2 and 3). This unit represents the basement for the region and has been dated at 1440 ±15 Ma by UPb in zircon (Anderson and Silver, 1977). The Cananea Granite is overlain by a Lower Paleozoic platform sequence (Figure 3), mostly quartzite and carbonatos, succeeded by the conformably overlying Upper Paleozoic carbonatos of the Naco Group (Meinert, 1982). All these rock units crop out extensively at the Cananea mine area and its vicinity; however, neither units have been recognized in the Milpillas area (Figure 4), but may well be present at a greater depth than the current drillcore exploration program.
The lowermost unit from the volcanic stratigraphy that crop out in the Cananea District (Figure 3) is the Late Triassic Early Jurassic Elenita Formation (Valentine, 1936), which consists of a sequence of volcaniclastic and sedimentary rocks that include rhyolitic flows and tuffs, interbedded with andesites, sandstones, quartzites and conglomerates. This unit can be correlated with the Mount Wrightson and Fresnal Canyon Formations from southern Arizona, which have been dated between 220 and 192 Ma (Tosdale et al. , 1989).
In the Milpillas area, one the main volcaniclastic host rock units is the Laramide Mesa Formation (Valentine, 1936), which unconformably overlies the Henrietta Formation (Figure 5). The Mesa Formation is a calcalkaline volcaniclastic unit that has an average thickness of1500 m, and extensively outcrops throughout the Cananea District where it has been dated at 69 Ma (Wodzicki, 1995). These volcanic rocks have a medium to high potassium content and consist of trachybasaltic to andesitic agglomerates, flows and tuffs, including dacite and trachydacite, with andesitic composition being dominant throughout the sequence. In the Cananea District, this unit commonly includes significant thicknesses of interbedded volcanic sandstones and agglomerates, as well as a unit of basaltic flows, synvolcanic diabase sills and domes, locally known as the Mariquita Formation (Valentine, 1936). The oldest volcanic unit that crops out at Milpillas belongs to the Jurassic Henrietta Formation (Valentine, 1936). This is a volcaniclastic sequence, which consists of calcalkaline dacitic and rhyolitic flows and tuffs, interbedded with agglomerates, latites and andesites (Wodzicki, 2001). In the Cananea region, this unit overlies the Elenita Formation (Figure 3). The Henrietta Formation has been correlated with the Artesa sequence from southern Arizona (Tosdal et al., 1989). Although none of these units have been isotopically dated, a Mid to Late Jurassic age (165 to 150 Ma) has been assigned to them (Wodzicki, 2001).
Small porphyry stocks that vary in composition from quartz monzonite to monzonite intruded the Henrietta and Mesa Formations (Figure 3 and 5). The porphyry stocks consist of 25 mm quartz, feldspar and biotite phenocry sts in a matrix of aphaniticfine quartz and orthoclase. The porphyry stocks are typically overprinted by strong sericitic alteration and are the main host to the Cu mineralization, but this Cu mineralization also extends into the immediate intruded volcaniclastic rocks. These porphyry stocks are spatially and could be genetically related to the late stages of the Laramide batholitic pluton complex locally known as the CuitacaTinajabatholith. This plutonic unit outcrops extensively throughout the Cananea Mining District. The CuitacaTinaja batolith is a granodiorite that contains biotite and hornblende as the main accessories, with minor magnetite and sphene. This pluton has been dated at 64 ± 3.0 Ma, using UPb in zircon (Anderson and Silver, 1977). No porphyry units crop out at the surface in the Milpillas area (Figure 5), however, there are some isolated outcrops of altered and leached volcanic host rocks. The ore body is completely covered by a sequence of post mineralization conglomerates and syntectonic gravels (Figures 2, 4, 5).
The structural control of PCDs emplacement in southwestern North America is consistent, at a district scale, with the dominant tectonic stresses that existed at their particular time of formation. These stresses vary from compressional to tensional (Titley, 2001). However, the tectonic evolution of this region has continued after ore deposit formation. During the relaxation of confining stresses at the North AmericanPacific plate margin due to changes in plate motions and/or plate margin configuration in the mid to late Tertiary (Gans and Miller, 1993; Basin and Range Province event), the region has been intensely faulted, extended and rotated, resulting in a significant disruption and rotation of deposits (e.g., San ManuelKalamazoo, Ajo, and Cananea). The magnitude of rotation varies from moderate (30° to 60°) to severe (60° to 90°) (Wilkins and Heidrick, 1995).
In the Milpillas area, three main lineaments have been described: a premineral NS trend, a synmineral NE trend, and a postmineral NW trend (de la Garza et al., 2003). However, a detailed structural study of the Milpillas deposit from quartz veins and mineralized structures performed by CarreónPallares (2002) shows a flat radial and concentric structural pattern with preferential dips to the NE, E and SE. These dip trends are the same primary main orientations reported for Laramide stocks throughout Arizona (Rehrig andHeidrick, 1972; Heidrick and Titley, 1982), whereas the concentric pattern has been recognized in Sierrita, Arizona (Titley, 1982).
Mineralization and alteration
The hypogene mineralization in PCDs from the district is mainly present as breccias, stockwork and/or disseminated sulfide minerals. Where preLaramide sedimentary host rocks are present, skarn mineralization developed. Highgrade, but low tonnage ore bodies, are found in skarn zones, as for example in the Cananea mine, where mineralization of CuZnPb was developed by replacement of Paleozoic carbonate rocks interbedded with quartzites (Meinert, 1982). In some deposits, high grade mineralization was developed in breccias pipes, such as in the Cananea mine (Brecha La Colorada, Bushnell, 1988) or in Maria mine (Wodzicki, 1995). At the Milpillas deposit, scarce and lowgrade hypogene or primary mineralization is recognized (0.150.20 % Cu) and because of these low grades, the exploration program focused on areas of supergene enrichment.
Most of the porphyry copper deposits in the Cananea District have been dated by KAr dating techniques, yielding ages from 60 ± 4 Ma to 54 ± 2 Ma (Damon and Mauger, 1966; Damon et al., 1983; Wodzicki, 1995).
The Milpillas deposit is a secondary enriched porphyry copper deposit that consists of highgrade chalcocite blankets that are entirely covered by TertiaryQuaternary alluvial sediments commonly 50250 meters thick (de la Garza et al., 2003). Milpillas was discovered and developed after intensive exploration programs and more than 100,000 meters of drilling, initially by Minera Cuicuilco in 1975 and continued up to feasibility in 1998 by Industrias Peñoles mining company.
The supergene enrichment zone presents a vertical zoning with an upper leach cap and oxide level typical of porphyry copper systems. The secondary enriched zones (Figure 5) comprise the most important ore bodies in the deposit. These bodies can reach copper grades that range from >1% to more than 10%.
Descriptions of supergene mineralization are scarce or nonexisting for Mexican PCDs. Seagart et al. (1974) provided the only known description of this type of mineralization in La Caridad. In the Milpillas ore body, the high grades of Cu are found in subhorizontal bodies or blankets (Figure 5). At least three cycles of secondary enrichment are recognized in the deposit (see Anderson, 1982; Titley and Marozas, 1995; and Gilmour, 1995 for review of leach capping processes and supergene copper enrichment), which resulted in at least six 'blankets' that occur at a depth of 150 to 750 meters below the surface. The upper three blankets contain oxide mineralization and have a complex mineralogical assemblage consisting of: "green Cuoxidescarbonatos" (antlerite, brochantite, malachite, azurite and chrysocolla); "red Cuoxides" (cuprite, native copper, delafossite, and minor "pitch" limonite); and "black Cuoxides" (neotocite, melaconite, tenorite, and minor "Cuwad") (de la Garza et al., 2003). Below these three blankets is an intermediate horizon that contains a mixture of oxides and sulfides. The two deepest blankets contain dominantly secondary sulfide minerals (mainly chalcocite and minor covellite; de la Garza et al., 2003). Total copper resources for these blankets are 30 million tons at 2.5% Cu.
Zircon UPb dating
A sample was collected from drill hole M120 at a depth of 540 m (Figure 5). The sample was crushed and milled. Heavy mineral concentrates of the <350 microns fraction were separated magnetically. Inclusionfree zircons from the nonmagnetic fraction were handpicked under a binocular microscope. Zircons were mounted in epoxy and polished for laser ablation analysis.
Single zircon crystals were analyzed in polished sections with a Micromass Isoprobe ICPMS multicollector equipped with nine Faraday collectors, an axial Daly detector, and four ioncounting channels (Dickinson and Gehrels, 2003). The Isoprobe is equipped with an ArF Excimer laser, which has an emission wavelength of 193 nm. The analyses were conducted on 5035 micron spots with output energy of 32 mJ and a repetition rate of 10 Hz. Each analysis consisted of a background measurement (one 20second integration on peaks with no laser firing) and twenty Isecond integrations on peaks with the laser firing. Any Hg contribution to the 204Pb mass is accordingly removed by subtracting the backgrounds values. The depth of each ablation pit was 20 microns. Total measurement time was 90 s per analysis.
The collectors were configured for simultaneous measurement of 204Pb in an ioncounting channel and 206Pb206,Pb208Pb232Th and 238U in Faraday detectors. All analyses were conducted in static mode. Interelement fractionation was monitored by analyzing fragments of SL1, a large concordant zircon crystal from Sri Lanka with a known (IDTIMS) age of 564 ± 4 Ma (2σ) (Gehrels, unpublished data). The reported ages for zircon grains are based entirely on the 206Pb/238U ratios because errors of the 207Pb/235U and 206Pb/207Pb ratios are significantly greater. The larger errors are the result of the low intensity (commonly <0.5 mV) of the 207Pb signal from these young, lowU grains. 207Pb/235U and 206Pb/207Pb ratios and ages are accordingly not reported.
The 206Pb/238U ratios are corrected for common Pb by using the measured 206Pb/204Pb, a common Pb composition from Stacey and Kramers (1975), and an uncertainty of 1.0 unit on the common 206Pb/204Pb.
The weighted mean of 16 individual analyses was calculated according to Ludwig (2003). The mean considers only the measurement or random errors (errors in 206Pb/238U and 206Pb/204Pb of each unknown). For this sample the random error is 0.6 Ma (2σ), and represents 1%. Age of standard, calibration correction from standard, composition of common Pb, decay constant uncertainty are the other sources that contributed to the error in the final age determination. These uncertainties are grouped and are known as the systematic error. For this sample the systematic error is 1.8%. The error in the age of the sample is calculated by adding quadratically the two components (random or measurement error and systematic error), which for this sample is 2.1 % (i.e., 1.3 Ma). All age uncertainties are reported at the 2sigma level (2σ).
Molybdenite ReOs dating
Molybdenum mineralization at Milpillas occurs frequently intergrown with primary copper sulfides. In order to determine the timing of hydrothermal mineralization, two molybdenite samples where selected from two different drill holes M120 (at 540 m depth) and M098 (at 514 m depth) (Figure 5). Molybdenite sample M120 was collected from a 4mmthick vein that has an assemblage of quartzsericitemolybdenite and sample M98 was collected from a 5mmthick vein with an assemblage of quartzsericitemolybdenitechalcopyritepyrite (Figure 6). Both samples are from the quartz monzonite porphyry unit, with a medium to strong quartzsericite alteration (Figure 4) that overprints and partially replaces the original rockforming silicates and their preexisting alteration products (e.g., biotite and Kfeldspar) (Beane, 1982).
The ReOs system applied to molybdenite is an important tool in determining the timing of mineralization since ore minerals (molybdenite) are dated directly. Other dating techniques, such as KAr and ArAr are applied to associated silicates and hence provide indirect age determinations. Furthermore, the very low errors obtained with the ReOs technique (between 0.33% to <1% of age determination) allow us to constrain or identify different pulses of mineralization that may occur in very short periods of time (e.g., Maksaev et al., 2004). However, there is a continuous debate regarding the possible opensystem behavior of Re and Os in molybdenite (see McCandless et al., 1993; Stein et al., 2001; Barra et al, 2003 for discussions).
Approximately 0.05 g of handpicked molybdenite and spikes were loaded in a Carius tube with 8 mL frozen reverse aqua regia. While the reagents, sample and spikes were frozen, the Carius tube was sealed and left to thaw at room temperature (Shirley and Walker, 1995). The tube was placed in an oven and heated to 240 °C for 12 hours. Osmium was separated from the solution in a twostage distillation process (Nagler and Frei, 1997). Osmium was further purified using microdistillation technique (Birck et al., 1997) and loaded on platinum filaments with Ba(OH)2 for thermal ionization mass spectrometer (TIMS). After osmium separation, the remaining acid solution was dried and redissolved in 0.1 HNO3. Rhenium was extracted and purified through a twostage separation column using AG1 X8 (100200 mesh) resin and loaded on nickel filaments with Ba(NO3)2 for TIMS measurements.
Samples were analyzed by negative thermal ion mass spectrometry (NTIMS) (Creaser et al., 1991) on a VG 54 mass spectrometer. Molybdenite ages were calculated using a 187Re decay constant of 1.6661011 year1(Smoliar et al, 1996). Ages are reported with a conservative total error of 0.5 % (2 sigma), which is a conservative approach that considers uncertainties from instrumental counting statistics, uncertainties in spike calibrations and in the 187Re decay constant (0.31%). Blank levels are less than 7 ppt Os and 15 ppt Re.
Zircon UPb results
Sixteen zircon grains were measured from sample M120. Results are reported in Table 1 and each line represents a spot analysis. All reported ages in Table 1 have uncertainties at the onesigma level (1σ), which only includes the measurement error.
Zircons analyzed are clear pinkish in color and range from 80 to 250 µm in size. They are doublyterminated prisms dominated by the  face with a 2.53:1 length to width ratio, which are typical morphologies of zircons in igneous rocks (Figure 7) Cathodoluminescence (CL) images show that the zircons have narrow zoning (Figure 7), which is characteristic of evolved magmas (Corfu et al., 2003). Measurements were made at the center and tips of zircon crystals.
Zircons from sample M120 have U and Th concentrations that vary from 530195 ppm and 24088 ppm, yielding U/Th ratios of 2, characteristic of igneous zircons (Rubatto, 2002). These zircons yielded a weighted average 206Pb/238U age of 63.9 ± 1.3 Ma (n=16, MSWD=0.91; Figure 8). In the sixteen grains analyzed, no older component was detected.
Molybdenite ReOs results
ReOs age determinations for two molybdenite samples are shown in Table 2. This table also includes previous data from the district reported by Barra et al. (in press). Sample locations are shown in Figure 4 and 5. Total rhenium and 187Os concentration range from 65478785 ppm and 43255805 ppb, respectively. Sample M120 yielded an age of 63.0 ± 0.4 Ma (0.5% error) and sample M098, 63.1 ± 0.4 Ma (0.5% error).
Age of mineralization
The 206Pb/238U zircon age of 63.9 ± 1.3 Ma (Figure 8) for the mineralized quartz monzonite porphyry unit is the only crystallization age reported so far for a productive intrusion in the Cananea District. This age is similar to the Cuitaca Granodiorite (64 ± 3 Ma) that crops out in the western border of the Cuitaca Graben. However, this unit has not been identified in any of the several drill holes from the Milpillas area.
Molybdenite samples of two different mineral assemblages from two deep drill holes (separated about 100 m from each other), have identical ReOs ages, suggesting that the molybdenite mineralization of Milpillas porphyry copper deposit occurred within a very short period of time (weighted average age of 63.1 ± 0.3 Ma).
Our UPb and ReOs ages indicate a temporal relationship between the magmatism and hy drothermal activity, and identify the Milpillas porphyry copper deposit as the oldest Laramide porphyry in the Cananea District. Furthermore, the limited data presented suggests that the duration of magmatichydrothermal activity in Milpillas was brief and that the hypogene mineralization was the product of a lowgrade single complex intrusion as proposed by Gustafson (2000).
Longlived or shortlived multiple mineralization centers
It is evident that knowledge of the age and duration of geologic events that result in the formation of important concentrations of ore minerals in the earth's crust is fundamental to our understanding of the evolution and origin of ore deposits. For porphyry copper deposits, the longlived magmatichydrothermal model versus the shortlived model, with several discrete pulses, and its role in the formation of large or giant ore deposits has become the focus of numerous recent studies (e.g. , Arribas et al., 1995; Cornejo et al, 1997; Marsh et al., 1997; Clark et al, 1998; Hedenquist et al, 1998; Reynolds et al, 1998; Selby and Creaser, 2001; Barra et al, 2003; Mastermanneet al.., 2004; Maksaev et al, 2004). Consequently, the determination of the lifespan of porphyry copper systems and its relation with the size of the deposit (i.e., the amount of copper contained) is critical in the development of genetic models of PCDs at the deposit level and probably more relevant at the district level were porphyries tend to occur in clusters. Obviously, timing information is relevant in the construction of regional metallogenic models.
The pioneering work of Damon et al. (1983) remained for many years the only geochronological source on Mexican PCDs. This work reported several KAr ages of different Krich minerals ( i.e. , hornblende, biotite, Kfeldspar) for host rocks and mineralized porphyries. However, more recent age determinations using other techniques have shown that some of the KAr ages of Damon et al. (1983) do not represent the main hydrothermalmineralization or magmatic episodes (i.e., El Arco Baja California, Mexico, KAr of 98106 Ma (Barthelmy, 1975) versus UPb and ReOs of 164 Ma (ValenciaGómez, 2005); Cumobabi KAr of 40 Ma compared to KAr of 55.663.1 Ma (Scherkenbach et al, 1985) and ReOs of 59 Ma (Barra et al., in press). These KAr ages apparently record cooling rather than magmatic or hy drothermal events, and therefore led to erroneous metallogenetic models of the region.
Porphyry copper deposits in the NorthAmerica southwest did not form during temporally random or isolated events, but rather during the maturation of complex magmatic centers that progressed through a longlived sequence of igneous episodes (Lang, 1991). The Cananea cluster, the largest porphyry CuMo district in Mexico, is interpreted to be the result of longlived magmatichydrothermal system, spanning from 64 Ma to 52 Ma (Figure 9, Meinert, 1982; Wodzicki, 1995). This statement was supported by the early less precise KAr and a ReOs molybdenite age (ICPMS; MaCandless et al, 1993), scarce UPb ages and limited ArAr geochronological data from different geological units from various deposits in the district. However, it is clear that the large span of time (> 10 Ma) in the magmatichydrothermal system might be a function of disturbed Ar or a less precise ReOs age.
Barra et al. (in press) dated several porphyry copper centers from Arizona, Sonora and Sinaloa. The new ReOs molybdenite ages were obtained from different centers of mineralization in the Cananea District, including El Alacrán prospect, former Maria mine and former breccia La Colorada and Incremento 3 at Cananea mines (Figure 2 and Table 2). This data, in addition to the new data from Milpillas indicate that mineralization within the district occurred in at least three discrete episodes, at 59 Ma, 61 Ma and 63 Ma (Figure 9), suggesting a model of multiple centers of mineralization produced during shortlived discrete periods of time.
Furthermore, it is possible that the large volume of metal in the Cananea mine is the result of overprinting of multiple discrete hydrothermalmineralization events, in constrastto single mineralization events in Maria, Milpillas and El Alacrán. The limited geochronological data for Cananea does not allow us to test this hypothesis, however, several examples from Chilean porphyry copper deposits (i.e., Chuquicamata, Reynolds et al, 1998; Ballard et al, 2001; Ossandon et al., 2001; Los Pelambres, Bertens et al., 2003, La Escondida, PadillaGarza et al., 2004; El Teniente, Maksaev et al., 2004) suggest that large deposits are the result of multiple overlapping of discrete mineralization episodes.
Timing of mineralization in Northwest Mexico
Porphyry copper mineralization in Northwest Mexico is Laramide in age (Damon et al., 1983), with the exception of El Arco in Baja California, which has an older Middle Jurassic age (164 Ma, ValenciaGómez, 2005).
The Laramide orogeny is characterized in the North American southwest by a compressional regime with basement uplift and thrust fault deformation, and widespread igneous activity, which produced extensive calealkaline magmatism in southern Arizona, New Mexico, and Sonora ranging from 80 Ma to 40 Ma (Damon et al., 1964; Damon andMauger, 1966; Coney, 1976; Shafiqullah et al., 1980; Damon et al, 1983). McCandless and Ruiz (1993) determined two distinct intervals of porphyry copper mineralization in the southwestern region (including northern Mexico), one from 7470 Ma and the other from 6055 Ma, based on ReOs systematics. However, in spite of this important and pioneering contribution, these ages were determined using less precise ICPMS technique, and ages were calculated with the old ReOs decay constant (1.64101 1 a1, Lindner et al., 1986), yielding results with high errors and slightly older ages. For example, the ReOs molybdenite age of Maria mine calculated at 57.4 ±1.6 Ma (1 sigma) is recalculated to 56.5 ± 3.2 Ma (2 sigma) using the latest ReOs decay constant of 1.6661011 a1(Smoliar et al, 1996). This age is very close to the new ReOs age determination from a sample from the same deposit using the more precise TIMS technique, which yielded an age of 60.4 ± 0.3 Ma (Barra et al, in press). This new determination and the small associated error, allow us to better constrain the relative timing of the different deposits in this important province. ReOs ages from a number of porphyry copper deposits in northwest Mexico: La Caridad (Valencia et al, 2005), El Crestón, Cananea, El Alacrán, Suaqui Verde, Maria, and Cuatro Hermanos (Barra et al., in press), and Milpillas (this study), suggests that the two largest districts in northwest Mexico occurred in two intervals; at 6359 Ma (Cananea District), and at 5553 Ma (La Caridad District). Although mineralization in these districts formed in two different episodes, magmatism seems to have occurred over a much more extensive period, overlapping in space and time. This is illustrated in La Caridad, where 63.5 Ma volcanic rocks host the 54 Ma porphyry copper mineralization (Valencia et al., 2005). Similar examples of this have been recognized in other PCDs in the Atizonan province.
Finally, the 70 Ma porphyry mineralization recognized in northern Arizona (e.g., Mineral Park, Titley, 1982; Bagdad, McCandless and Ruiz, 1993; Barra et al., 2003) has not yet been recognized in northwestern Mexico.
UPb zircon analyses from the mineralized quartz monzonite porphyry at the Milpillas deposit yielded a 206Pb/238U age of 63.9 ± 1.3 Ma. This age coupled with molybdenite ages from two deep drill holes which have identical ReOs ages (weighted average age of 63.1 ± 0.3 Ma), suggests that the mineralization of Milpillas porphyry copper deposit occurred within a short period of time.
Mineralization within the Cananea District occurred in at least three discrete periods, at 59 Ma, 61 Ma and 63 Ma, supporting the model of multiple centers of mineralization produced by the short lived discrete periods rather than a long lived period of mineralization.
We suggest that the large volume of metal in the Cananea mine could result from the overprinting of multiple discrete periods of hydrothermal mineralization, contrasting with single mineralization event as in Maria, Milpillas and El Alacrán.
The largest mineralized districts in northwest Mexico occur in two main intervals, one at 5963 Ma (Cananea), and the other at 5355 Ma (La Caridad District), where associated magmatism overlaps in space and time.
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