Exploration Tools for Linked Porphyry and Epithermal Deposits: Example from the Mankayan Intrusion-Centered Cu-Au District, Luzon, Philippines*

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Exploration Tools for Linked Porphyry and Epithermal Deposits: Example from the Mankayan Intrusion-Centered Cu-Au District, Luzon, Philippines* Economic Geology, v. 106, pp. 1365–1398 Exploration Tools for Linked Porphyry and Epithermal Deposits: Example from the Mankayan Intrusion-Centered Cu-Au District, Luzon, Philippines* ZHAOSHAN CHANG,1,†,** JEFFREY W. HEDENQUIST,2 NOEL C. WHITE,3 DAVID R. COOKE,1 MICHAEL ROACH,1 CARI L. DEYELL,1 JOEY GARCIA, JR., 4,** J. BRUCE GEMMELL,1 STAFFORD MCKNIGHT,5 AND ANA LIZA CUISON4,*** 1 CODES ARC Centre of Excellence in Ore Deposits, University of Tasmania, Private Bag 126, Hobart, Tasmania 7001, Australia 2 99 Fifth Avenue-Suite 260, Ottawa, Ontario, Canada K1S5P5 3 P.O. Box 5181, Kenmore East, Queensland 4069, Australia 4 Lepanto Consolidated Mining Company, 21st Fl., BA-Lepanto Bldg., 8747 Paseo de Roxas, 1126, Makati City, Philippines 5 Geology and Metallurgy, School of Science and Engineering, University of Ballarat, P.O. Box 663, Ballarat VIC 3353, Australia Abstract The Mankayan mineral district of northern Luzon, Philippines, hosts several significant ore deposits and prospects of various types within an area of ~25 km2, including the Far Southeast porphyry Cu-Au deposit, the Lepanto high sulfidation epithermal Cu-Au deposit, the Victoria intermediate sulfidation epithermal Au-Ag vein deposit, the Teresa epithermal Au-Ag vein deposit, the Guinaoang porphyry Cu-Au deposit, and the Buaki and Palidan porphyry Cu-Au prospects, all having formed in a period of about 2 m.y., from ~3 Ma. The geo- logic units include (1) a basement composed of Late Cretaceous to middle Miocene metavolcanic rocks and volcaniclastic rocks; (2) the Miocene 12 to 13 Ma tonalitic Bagon intrusive complex; (3) the Pliocene, ~2.2 to 1.8 Ma, Imbanguila dacite porphyry and pyroclastic rocks; and (4) postmineralization cover rocks, including the ~1.2 to 1.0 Ma Bato dacite porphyry and pyroclastic rocks and the ~0.02 Ma Lapangan tuff. Extensive advanced argillic alteration crops out for ~7 km along the unconformity between the basement rocks and the Imbanguila dacite formation and consists of quartz-alunite ± pyrophyllite or diaspore, with local zones of silicic alteration and a halo of dickite ± kaolinite. The alteration and its subhorizontal geometry indi- cate that it is a lithocap or coalesced lithocaps. The northwest-striking portion is ~4 km long and hosts the Lepanto enargite Au ore deposit, also controlled by the Lepanto fault. The Lepanto epithermal deposit is related to the underlying Far Southeast porphyry; the quartz-alunite alteration halo of Lepanto is contempo- raneous with the ~1.4 Ma potassic alteration of the porphyry. There are also silicic-advanced argillic alteration patches ~600 m above the Far Southeast orebody at the present surface; these are interpreted to be perched alteration. There is no systematic mineralogical or textural zoning in the Lepanto lithocap that indicates direc- tion to the intrusive source. Most surface samples of the lithocap contain less than 50 ppb Au, despite many being less than a few hundred meters from underground Cu-Au ore. This study found that several characteristics of the Lepanto lithocap change systematically with distance from the causative intrusion: The alunite absorption peak at ~1,480 nm in the short wavelength infrared (SWIR) spectrum shifts to higher wavelengths where the sample is closer to the intrusive center, due to higher Na and lower K content in the alunite; published experimental studies indicate that high Na/(Na + K) is related to higher formation temperature. High Ca alunite, including huangite, also occurs at locations proximal to the intrusive center. Alunite mineral composition analyzed by laser ablation-inductively coupled plasma-mass spec- trometry (LA-ICP-MS) indicates that the Pb content decreases toward the intrusive center, whereas Sr, La, Sr/Pb, and La/Pb increase markedly. Whole-rock compositions, using only nonmineralized (taken as Cu <0.1wt % and Au <0.1 ppm) and alunite-bearing samples, show that Pb and Ag/Au, plus Hg and Ag, decrease toward the intrusive center, and Sr/Pb and La/Pb ratios increase. Normalizing whole-rock Pb to the (Na + K) molal content produces a proxy for the alunite mineral composition, and this ratio provides the same indications as the LA-ICP-MS analyses of alunite. The concealed Victoria epithermal veins consist of intermediate sulfida- tion mineralization on the southwest flank of the porphyry. The veins are not exposed, but their presence at depth is indicated by subtle alteration (illite or interstratified illite and/or smectite or smectite + pyrite) and geochemical (As, Se) anomalies at the surface. The anomalies are strongly dependent on erosion level; no anomalies were found where the surface is >~350 m above the upper extent of the veins. An airborne geo- physics survey indicates that the Far Southeast orebody is associated with a wide zone of demagnetization due to extensive magnetite-destructive phyllic alteration. Such low magnetic anomalies on the margin of a large lithocap elsewhere may deserve attention. The directional indicators and mineralization signatures found in this study have the potential to indicate direction to the intrusive center during exploration of similar porphyry- epithermal districts. † Corresponding author: e-mail, [email protected] *A digital supplement to this paper is available at <http://economicgeology.org/> **Current address: School of Earth and Environmental Sciences, James Cook University, Townsville, QLD 4811, Australia. ***Current address: CODES ARC Centre of Excellence in Ore Deposits, University of Tasmania, Private Bag 126, Hobart, Tasmania 7001, Australia. © 2011 Gold Open Access: this paper is published under the terms of the CC-BY license. 0361-0128/11/3995/1365-34 1365 Downloaded from http://pubs.geoscienceworld.org/segweb/economicgeology/article-pdf/106/8/1365/3968435/1365-1398.pdf by guest on 23 September 2021 1366 CHANG ET AL. Introduction such deposits (e.g., Sillitoe and Hedenquist, 2003; Sillitoe, LITHOCAPS are horizontal to subhorizontal blankets of resid- 2010) and evidence for transitions between them (e.g., Ein- ual quartz and advanced argillic alteration of hypogene origin, audi et al., 2003). occurring over intrusions (Sillitoe, 1995a). They can host high Discovery histories of ore deposits in the district sulfidation epithermal mineralization, particularly within their fracture-controlled roots. Lithocaps are temporally and The Lepanto enargite Au orebody was worked for Cu and th genetically related to intrusions that may be associated with Au at the start of the Ming dynasty (14 century), and by the deeper porphyry-style mineralization (Sillitoe, 1995a, 1999, local people prior to the 1500s, after which the Spanish be- 2011; Hedenquist et al., 1998). Lithocaps can have large areal came involved. Outcrops consisting of vuggy to massive extent (>20 km2; Sillitoe, 1995a) and, because they resist ero- quartz along the Lepanto fault were first mined near the sion, are typically prominent at the surface, which generally 1,150-m-elevation level, with luzonite-enargite still visible in makes them easy to find. The presence of a lithocap of large the old workings in the cliff face (Lepanto is the type locality areal extent (A. Arribas, pers. commun., 1999) is encouraging for luzonite). The Cantabro-Filipino company was the first to for exploration at an early stage, as it indicates extensive hy- conduct large-scale mining in 1865, with at least 1,100 metric drothermal activity and potential for high sulfidation ore; in tons (t) of Cu produced during a 10-year period. The present addition, there is potential for deeper porphyry and marginal underground mining activity dates from 1936, when the Lep- epithermal vein mineralization. Despite the relative ease of anto Consolidated Mining Co. commenced mining until the finding lithocaps, it may be difficult to further define the loca- Japanese took over production; Mitsui produced 11,000 t of tion of mineralization within, under, or adjacent to a large Cu during the early 1940s. Lepanto Consolidated Mining Co. lithocap due to the lack of directional indicators. In particular, resumed mining in 1948, and up to 1996 a total of 36.3 Mt of determining the position of the underlying intrusive center is ore was produced from the Lepanto mine at an average grade commonly difficult. In addition, veins on the margin may ter- of 2.9 percent Cu, 3.4 g/t Au, and 14 g/t Ag, with a total of minate several hundred meters below the paleosurface, 0.74 Mt Cu, 92 t Au, and 393 t Ag recovered. The Lepanto below the level of the lithocap. In a district without outcrop- mine closed in 1996 with a remaining minable reserve of 4.4 ping veins, exploration for such veins is typically difficult. Mt at 1.76 wt percent Cu and 2.4 g/t Au (Claveria et al., The Mankayan mineral district, northern Luzon, Philip- 1999a). pines, was studied in order to develop tools for exploration in The Far Southeast porphyry was discovered in 1980, based such districts, as it is the site of several large intrusion-related in part on the prediction that Lepanto was sitting over a por- ore deposits and prospects. The district lies within a well-de- phyry environment (Sillitoe, 1983). Porphyry fragments at the fined, 150-km-long belt of porphyry Cu deposits in the Cen- surface were recognized by Lepanto geologists in outcrops of tral Cordillera of northern Luzon (e.g., Cooke et al., 2011; Imbanguila dacite volcanic products in the 1970s. In 1978, Deyell and Hedenquist, 2011; Hollings et al., 2011a, b; Wa- the deeper parts of two drill holes, drilled in 1974 about 4 km ters et al., 2011; Wolfe and Cooke, 2011). It is one of the southeast of Lepanto, were recognized to contain porphyry- country’s richest mining districts, both in terms of proven and type mineralization; subsequent reassay in mid-1980 identi- potential economic value as well as abundance and diversity fied “appreciable Cu values” (Sillitoe, 1995b, p.
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