2010_apv

NI 43‐101 Technical Report, Dominican Republic

Minera Camargo S.A. de C.V. Page | 1

IINNDDEEPPEENNDDEENNTT TTEECCHHNNIICCAALL RREEPPOORRTT FFOORR TTHHEE AAMMPPLLIIAACCIIOONN PPUUEEBBLLOO VVIIEEJJOO ((AAPPVV)) PPRROOJJEECCTT,,

DDOOMMIINNIICCAANN RREEPPUUBBLLIICC LLaattiittuuddee 1188ºº5544'',, LLoonnggiittuuddee 7700ºº0066''

View of the Pueblo Viejo gold mine from Silica Ridge, La Cuaba lithocap.

Effective Date: Monday 23 August 2010

For

EVERTON RESOURCES: EVR TSX‐V #103‐5420 Canotek Road, Ottawa, Ontario, Canada K1J 1E9

Tel: 1‐800‐564‐6273; Fax: 1‐888‐453‐0330

By

M. Robinson, MASc., P.Eng Lic. # 23559, APEGBC. Minera Camargo S.A. de C.V.

E‐mail: [email protected]



Contents Table of Figures ................................................................................................................................................................. 3

List of Tables ..................................................................................................................................................................... 5

1.0 Summary ..................................................................................................................................................................... 6

2.0 Introduction ................................................................................................................................................................. 7

3.0 Reliance on other experts ............................................................................................................................................. 7

4.0 Property Description and Location ............................................................................................................................... 8

4.1 Essentials of the mining law in the Dominican Republic............................................................................................ 8

4.2 Environmental Permits .......................................................................................................................................... 10

5.0 Accessibility, Climate, Local Resources, Infrastructure and Physiography .................................................................. 10

6.0 History ....................................................................................................................................................................... 11

7.0 Geological Setting ...................................................................................................................................................... 12

7.1 Regional Geology ................................................................................................................................................... 12

7.2 Property Geology ................................................................................................................................................... 13

7.2.1 Maimón Formation ......................................................................................................................................... 13

7.2.2 Los Ranchos Formation ................................................................................................................................... 14

7.2.3 Hatillo Formation ............................................................................................................................................ 14

7.2.4 Las Lagunas Formation ................................................................................................................................... 15

7.2.5 Peralvillo Formation ........................................................................................................................................ 15

7.2.6 Late Cretaceous to Tertiary diorite/dacite intrusions ....................................................................................... 15

8.0 Deposit Types ............................................................................................................................................................ 18

8.1 Volcanogenic massive sulfide deposits ................................................................................................................... 18

8.2 Porphyry copper systems ....................................................................................................................................... 19

8.3 Epithermal gold deposits ....................................................................................................................................... 20

9.0 Mineralization ............................................................................................................................................................ 21

9.1 Tres Bocas gold‐rich VMS prospect ........................................................................................................................ 21

9.2 Cuance gold‐rich VMS prospect ............................................................................................................................. 22

9.3 Los Hojanchos ........................................................................................................................................................ 24

9.4 La Lechoza (VMS?) ................................................................................................................................................ 26

9.5 La Cuaba Lithocap ................................................................................................................................................. 28

10.0 Exploration ............................................................................................................................................................... 32

10.1 Airborne Geophysical Surveys .............................................................................................................................. 32

10.2 Soil Geochemistry ................................................................................................................................................ 36

10.3 Rock Geochemistry .............................................................................................................................................. 38

10.4 Lithocap Alteration Study using a PIMA SWIR spectrometer ................................................................................ 39

11.0 Drilling ...................................................................................................................................................................... 42



11.1 Percussion Drilling ................................................................................................................................................ 42

11.2 Diamond Drilling .................................................................................................................................................. 43

12.0 Sampling Method and Approach .............................................................................................................................. 45

12.1 Soil Samples ......................................................................................................................................................... 45

12.2 Rock Samples ....................................................................................................................................................... 46

12.3 Percussion Drill Samples....................................................................................................................................... 46

12.4 Diamond Drill Samples ......................................................................................................................................... 46

13.0 Sample Preparation, Analysis and Security ............................................................................................................... 47

13.1 Soil samples .......................................................................................................................................................... 47

13.2 Percussion drill samples ........................................................................................................................................ 47

13.3 Rock and core samples: ........................................................................................................................................ 47

14.0 Data Verification ...................................................................................................................................................... 48

15.0 Adjacent Properties .................................................................................................................................................. 49

15.1 Pueblo Viejo ......................................................................................................................................................... 49

15.2 Cerro de Maimón .................................................................................................................................................. 50

16.0 Mineral Processing and Metallurgical Testing ........................................................................................................... 51

17.0 Mineral Resource Estimates ...................................................................................................................................... 51

18.0 Other Relevant Data and Information....................................................................................................................... 51

19.0 Interpretation and Conclusions ................................................................................................................................. 51

20.0 Recommendations ................................................................................................................................................... 52

21.0 References ............................................................................................................................................................... 55

Certificate of Author ........................................................................................................................................................ 58

Appendix 1: Abbreviated listing of surface rock data ........................................................................................................ 59

Appendix 2: Abbreviated listing of Core Samples ............................................................................................................. 61

Appendix 3: Assay certificates for surface rock samples and six ¼ core check samples ......... Error! Bookmark not defined.

Table of Figures

Fig. 4.1 Concession map of the Property. ........................................................................................................................... 9

Fig. 7.1 Regional Geological Map of the Island of Hispaniola ............................................................................................ 13

Fig. 7.2 Geological Legend ............................................................................................................................................... 17

Fig. 7.3 Geological compilation map of the Property ........................................................................................................ 17

Fig. 8.1 Essential characteristics of an idealized gold‐rich volcanogenic massive sulfide deposit.. .................................... 19

Fig. 8.2 Essential characteristics of a porphyry copper system ......................................................................................... 20

Fig. 8.3. Generalized alteration‐mineralization zoning pattern for porphyry copper deposits (from Sillitoe, 2010). .......... 20

Fig. 9.1 Cross‐section through Tres Bocas ........................................................................................................................ 22



Fig. 9.2 Cross‐section through Cuance ............................................................................................................................. 24

Fig. 9.3 Cross‐section through Los Hojanchos .................................................................................................................. 26

Fig. 9.4 Cross‐section through La Lechoza, North Hill ...................................................................................................... 28

Fig. 9.5 Cross‐section through La Cuaba .......................................................................................................................... 29

Photo 9.1. TRES BOCAS. Rare surface outcrop of quartz‐kaolinite schist ......................................................................... 30

Photo 9.2. TRES BOCAS. Photograph of banded massive sulfide ..................................................................................... 30

Photo 9.3. CUANCE. Rhyolite lapilli tuff in the hanging wall to the Cuance VMS prospect. .............................................. 30

Photo 9.4 CUANCE. View of the Cuance VMS horizon .................................................................................................... 30

Photo 9.5 CUANCE. Sample 167239 ................................................................................................................................ 30

Photo 9.6. CUANCE. Photomicrograph of sample 167282 ............................................................................................... 30

Photo 9.6. LOS HOJANCHOS. Quartz veinlets with red Fe‐oxide. .................................................................................... 31

Photo 9.7. LOS HOJANCHOS. YAM PIT – site of Pan Ocean DDH. ................................................................................. 31

Photo 9.8 LA LECHOZA. Ferruginous gossan at Spanish Pit. ........................................................................................... 31

Photo 9.9 LA LECHOZA. Ferruginous gossan at North Hill. .............................................................................................. 31

Photo 9.10 LA LECHOZA. Sample 311079 from APV 10‐02 .............................................................................................. 31

Photo 9.11 LA LECHOZA. Sample 311516 from APV 10‐07 .............................................................................................. 31

Photo 9.12 LA LECHOZA. Photomicrograph of sample 311268 ........................................................................................ 32

Photo 9.13 LA LECHOZA. Photomicrograph of sample 313262, APV 09‐15, 70‐71.2 m. .................................................... 32

Photo 9.14 LA CUABA. Silica and goethite matrix breccia ............................................................................................... 32

Photo 9.15 LA CUABA. Sample 36243, APV 04‐08, 176‐178 m. ....................................................................................... 32

Fig.10.1 Gridded airborne magnetic data ......................................................................................................................... 34

Fig.10.2 Map of amplitude of dB/dt Z channel 9. .............................................................................................................. 35

Fig. 10.3 Soil anomaly map for Loma El Mate, Los Hojanchos and Cuance. ...................................................................... 37

Fig. 10.4 Soil anomaly map for La Lechoza. ..................................................................................................................... 38

Fig. 10.6. Cross‐section through La Cuaba Lithocap. ....................................................................................................... 42

Photo 11.1. AIRTRACK DRILL. .......................................................................................................................................... 44

Photo 11.2. MAN PORTABLE DRILL RIG .......................................................................................................................... 44

Fig. 11.1 Drill collar location plan. ..................................................................................................................................... 45

Photo 15.1. PUEBLO VIEJO. Argillic altered Zambrana rhyolite dome. ............................................................................ 50

Photo 15.2 PUEBLO VIEJO. Photo of laminated massive sulphide protore ....................................................................... 50

Photo 15.3 PUEBLO VIEJO. Fairly flat lying carbonaceous quartz‐crystal tuff. ............................................................... 50

Photo 15.4 PUEBLO VIEJO. View of sub‐vertical diorite dike. .......................................................................................... 50

Fig. 20.1 Exploration diamond drilling plan . ................................................................................................................... 54



List of Tables Table 4.1 Summary description of the APV Project Exploration Concessions. .................................................................... 8

Table 9.1 Drill intercepts from Tres Bocas. ....................................................................................................................... 21

Table 9.2 Drill intercepts from Cuance. ............................................................................................................................ 23

Table 9.3 Drill intercepts from Los Hojanchos. ................................................................................................................. 25

Table 9.4 Drill intercepts from La Lechoza. ...................................................................................................................... 26

Table 9.5 Drill intercepts from La Cuaba. ......................................................................................................................... 29

Table 10.1 Summary distribution statistics for 8576 soil samples. ..................................................................................... 36

Table 10.2 Summary distribution statistics for 3974 rock samples. ................................................................................... 39

Table 12.1 Types of rock samples used to evaluate mineral occurrences on the Property. ............................................... 46

Table 14. 1 Repeat ¼ core samples. ................................................................................................................................. 49

Table 20.1 Summary of proposed Phase 1 Exploration Expenditures ................................................................................ 53

Table 20.2 Summary of proposed Phase 2 Exploration Expenditures ............................................................................... 53



1.0 Summary The Ampliación Pueblo Viejo (APV) Project is comprised of five contiguous mineral concessions totaling 16810 Ha centered 10 kilometers south of the city of Cotuí, in the central portion of the Dominican Republic, Island of Hispaniola, northern Caribbean Sea (Fig. 4.1). Four of the concessions are 50% owned and operated by Everton Minera Dominicana S.A., the Dominican subsidiary of Everton Resources (“Everton”). Joint venture partner Globestar Mining owns 50% of two of the concessions (Cuance and Los Hojanchos), and Linear Gold owns 50% of two other concessions (La Cueva and Ampliación Pueblo Viejo). Everton owns 100% of one concession (Jobo Claro). The APV concessions surround the Pueblo Viejo gold deposit in all directions except south. Past production from Pueblo Viejo is estimated at 27 million tonnes of oxide ore averaging 4.23 g/t Au and 21.6 g/t Ag (Kesler et al., 1981). The latest published reserve estimate for Pueblo Viejo is 248.6 million tonnes of ore grading 2.8 g/t Au, 13.4 g/t Ag, 0.56% Zn and 0.08% Cu (measured and indicated categories at a 1.4 g/t Au cut‐off grade; Smith et al., 2008). Partners Barrick Gold Corporation and Goldcorp Inc. are currently constructing an open‐pit mining complex on the site (cover photo). Current plans are to have the mine in production by the end of 2011 (Barrick Gold Corporation Annual Report, 2009).

The concessions overlap part of the Los Ranchos and Maimón Formations. Los Ranchos Formation represents the remnants of an Early Cretaceous axial primitive island arc, and Maimón Formation represents the fore‐arc volcano‐sedimentary basin. These rocks are overlain by Hatillo Formation limestone, La Laguna argillite, and deformed by thrust faulting. Finally, they are cross‐cut by Late Cretaceous to Tertiary diorite plutons.

Two ages of mineralization are thought to occur on the Property: (i) syn‐depositional volcanogenic massive sulphide (VMS) deposits of Early Cretaceous age in the Los Ranchos and Maimón Formations, and (ii) epigenetic gold vein deposits that are probably related to an unexposed Late Cretaceous or Tertiary porphyry copper‐gold system. On Everton’s Property such a porphyry might be centered below La Cuaba lithocap, an eroded zone of quartz‐pyrophyllite (advanced argillic) alteration that was originally about 1000 meters thick, and is typical of the upper parts of porphyry copper systems (Sillitoe, 2010). The lithocap is centered on a complex magnetic anomaly about 3.5 kilometers across that might mark the location of the causative porphyry intrusion in the sub‐surface. Pueblo Viejo is a giant gold deposit, and about 40% of giant deposits are intrusion‐centered (Hedenquist and White, 2005). Another factor that probably contributed to the unusual size of Pueblo Viejo is that the gold‐bearing veins cross‐cut a layer of rocks rich in syn‐sedimentary sulfides and biogenic carbon (Pueblo Viejo Member; Fig. 15.2). Both sulfides and carbon will react with any gold in solution and cause it to precipitate into the rock (Kesler et al., 1981).

North and west of Pueblo Viejo, several VMS prospects have been identified on the APV project: (i) La Lechoza, (ii) Cuance, (iii) Los Hojanchos and (iv) Tres Bocas. Of these, La Lechoza is the best defined, and there is near‐term potential to develop a polymetallic resource there with additional drilling down dip of the known intercepts. However, the most compelling VMS story is the zoned but untested geochemical anomaly in the area of historic Pan‐Ocean drill holes at Los Hojanchos. In this area, anomalous zinc and copper geochemistry defines an area about 2 kilometers long and 1.3 kilometers wide, with copper‐rich geochemistry occurring to the northeast (in the footwall), and zinc‐rich geochemistry below a basalt flow in the hanging wall (Figs. 9.3 and 10.3).

Everton is in the process of exploring the Property and has completed 16044.63 meters of drilling in 141 diamond drill holes, 2192 line kilometers of helicopter‐borne magnetic and electromagnetic geophysical surveys, several ground geophysical and geochemical surveys, and short‐wave infrared (SWIR) mineral determinations for 1995 surface rock samples and 665 core samples from La Cuaba lithocap. Some of the better diamond drill intercepts include: (i) 0.6 g/t Au, 48 g/t Ag, 0.9% Cu and 0.8% Zn across 21 m (APV 10‐07; La Lechoza), (ii) 0.3 g/t Au, 19 g/t Ag, 0.2% Cu and 3.1% Zn across 22.3 m (TBM‐26; Tres Bocas), and (iii) 1.1 g/t Au, 3 g/t Ag, 0.3% Cu and 2.0% Zn across 18 meters (CUA‐04; Cuance).

Everton Minera Dominicana’s core business plan for 2010‐2012 is twofold: (i) drill through the lithocap and explore for on‐strike and down‐dip extensions to Pueblo Viejo as that could be where the highest potential value of the Project is located, and (ii) explore and expand the known VMS mineralization elsewhere on the Property, mainly by drilling. The Budget allows for the use of a D‐6 tractor to build access roads and drill pads, although it may be easier from a permitting perspective to use a man portable drill in some locations. Overall, two phases of exploration drilling are planned. The first phase consists of 11 280 meters of drilling in 76 holes, with a maximum hole depth of 450 meters. Overall Phase 1



costs are estimated to be $4.0 million USD (Table 20.1). The second phase of drilling consists of 18 035 meters of drilling in 43 holes, with a maximum hole depth of 900 meters. The decision to attempt the deeper holes through the lithocap depends on the results of the first phase of drilling. Alternatively, the Phase 1 results might justify upgrading one of the prospects to an NI 43‐101 compliant mineral resource estimate. Overall, Phase 2 costs are estimated to be about $6.0 million USD (Table 20.2).

2.0 Introduction Minera Camargo S.A. de C.V. ("MCA") was retained by Marc L’Heureux of Everton Resources ("EVR: TSX‐V") to conduct an independent technical review and to prepare a report in compliance with National Instrument 43‐101 ("NI 43‐101") on the Ampliación Pueblo Viejo Project ("the Property") in the central Dominican Republic. The review is required by the TSX Venture Exchange as part of the documentation required for financing the Project.

The author has reviewed all of the technical information provided by Everton Resources. Sources of data include:

A Technical Report by Geo‐Habilis Consultants Inc. dated September 2006.

Several internal Technical Reports.

Geochemical data for 3989 rock samples and 8576 soil samples.

Magnetic and electromagnetic data from a 2192 line kilometer helicopter airborne geophysical survey flown over the Property by Fugro Airborne Surveys in 2007.

Maps for ground geophysical surveys.

Drilling Logs for 16044.63 meters of drilling in 141 diamond drill holes as well as assays for 8305 drill‐core samples.

SWIR mineral determinations for 1995 surface rock samples and 665 core samples from La Cuaba lithocap.

52.9 gigabytes of information in 72,829 electronic data files.

A 5 day field inspection was carried out by the author between 20 and 24 April 2010 in the company of Ing. H. Dominguez, Ing. Carlos Carrasco and Everton Minera Dominicana support personnel. The author collected 34 rock chip samples, 6 repeat ¼ core samples and 113 small half‐core samples to verify the general tenor of the mineralization and characterize the alteration mineralogy. Structural measurements were collected at all measurable outcrops, and some drill‐hole collar locations were confirmed. An inspection of different locations on the recently completed soil grid was also completed, and the author has walked parts of this grid to ensure that sample locations are correctly reported and that appropriate material was sampled.

In Minera Camargo’s laboratory, the rock and core samples were scanned using a Niton GOLDD XRF analyzer, and Terraspec SWIR spectrometer, as well as visually inspected using a Meiji binocular microscope. Magnetic susceptibility was measured with a Kappa magnetic susceptibility meter. Petrographic descriptions and analytical results were recorded (Appendices 1 and 2). Alteration assemblages were classified according to Gifkins (2005) for rocks from volcanogenic massive sulfide (VMS) prospects and according to Hauff (2005) for unclassified or epithermal vein prospects. The rock samples were then re‐packaged and sent to ACME Analytical Laboratories in Guadalajara for Au fire assays and ICP multi‐element analysis (Groups 1DX, Group 6 and Group 7; Appendix 3).

Drill hole data and surface geological plans from Everton’s database were not consistent. In order to present the Property geology and the geological context of the mineralization in Sections 7, 8 and 9, Minera Camargo drafted a new geological compilation map (Figure 7.2) using: (i) our own surface observations, (ii) all geological information from the drill hole logs, (iii) Everton’s rock sample observations, (iv) Everton’s mapping, and (v) government Sysmin geological maps as well as information from Childe (2000), Holbek and Daubney (2000), and Lewis et al. (2000).

3.0 Reliance on other experts It was not within the scope of this report to examine in detail or to independently verify the legal status or ownership of the Property. Everton Resources has not provided copies of title documents, Option Agreements or payment receipts. The author has reviewed the material regarding some of the land tenure obligations available on the Company website and on SEDAR, and has no reason to believe that ownership and status are other than as has been represented, but determination of secure mineral title is solely the responsibility of Everton Resources.



4.0 Property Description and Location The Ampliación Pueblo Viejo (APV) Project is comprised of five contiguous mineral concessions totaling 16810 Ha centered 10 kilometers south of the city of Cotuí, in the central portion of the Dominican Republic, Island of Hispaniola, northern Caribbean Sea (Fig. 4.1). The concessions are operated by Everton Minera Dominicana S.A., the Dominican subsidiary of Everton Resources.

Table 4.1 Summary description of the APV Project Exploration Concessions.

Property Owner Resolution

(Mining title)

Expiry Area (Ha)

Everton Interest

Ampliación Pueblo Viejo II (APV)

Linear Gold Caribe1 S.A. IX‐09 April 7, 2014 4045 Joint Venture with Linear Gold to

earn up to 65%.2

Jobo Claro II Everton Minera Dominicana, S.A.

In progress5 Approx. 2012 5030 100%. Purchased from Jose A

Bencosme 6 Aug 2007.

La Cueva (formerly Loma El Mate)

Linear Gold Caribe1 S.A. XII‐07 13‐Dec‐12 3395 50% Joint Venture with Linear Gold.

4

Los Hojanchos Corp. Minera Dominicana

3

In progress (?)

6

Approx. 2012 2400 50% Joint Venture with Globestar Mining

Cuance Corp. Minera Dominicana

3

LXXXVIII‐06 10‐Apr‐11 1940 50% Joint Venture with Globestar Mining

TOTAL 16810 1Linear Gold Caribe S.A. is a 100% subsidiary of Linear Gold Corp (now Brigus Gold Corp.). 2The Company can earn an undivided 50% interest in the APV Concession from Linear Gold by making cash payments totalling US$700,000, performing minimum Work of US$2,500,000 and issuing 1,200,000 Everton common shares over a three‐year period. The Company can acquire a 65% interest in the concession by incurring all additional expenditures on the concession to the completion of a bankable feasibility study and by paying Linear US$2,000,000 and issuing 1,000,000 additional Everton common shares. 3Corporacion Minera Dominicana S.A. is a 100% owned subsidiary of Globestar Mining. 4Since December of 2005, a 50% joint venture has been enforced by the partners. The joint venture is participatory with a dilution clause ultimately leading to a 2% NSR when participation drops below 10%. Everton is the current operator of the joint venture. 5On 4 March 2010 the five year term of the original Jobo Claro concession expired. A re‐application was submitted 1 March 2010 to the Dirección General de Minería. 6Corporacion Minera Dominicana S.A. has re‐applied for this concession, and the abstract of the application has been published.

4.1 Essentials of the mining law in the Dominican Republic

Important components of mining law (Ley 146, 1974) are:

Filing of an application involves two publications in a Dominican newspaper and the annual payment of fees.

All mining titles are to be delivered to a Dominican Republic company. Exploration titles may also be delivered to individuals or a foreign company, with certain exceptions (e.g. government employees or their immediate relatives and foreign governments).

Resolutions granting mineral title are issued by the Secretaría de Estado de Industria y Comercio (currently Ministry of Industry and Commerce) following a favorable recommendation by the Dirección General de Minería.

A company may have exploration and mining titles over a maximum of 30,000 hectares. An exploration title is valid for 3 years and may be followed by two one‐year extensions. At the end of the 5‐year period, the owner of the title applies for an exploitation permit, or a new round of exploration permitting may be started at the discretion of the mining department.

An agreement must be reached with surface rights owners (formal or informal) for each phase of exploration work. If mining is envisioned, land must be bought. A procedure exists in which government mediation is used to resolve disagreements, and this process may ultimately end in expropriation at a fair price.

Legal descriptions of exploration and mining concessions are based on polar co‐ordinates relative to a surveyed monument. The monument location is defined in UTM co‐ordinates, NAD27 datum. The concession boundaries are not marked or surveyed.



Fig. 4.1 Concession map of the Property showing producing mines Pueblo Viejo and Cerro de Maimón (bold), mineral prospects (pink) and diamond drill intercepts (red). Traverses made by the author are in grey. Red hatch shows the Loma La Cuaba lithocap. UTM NAD27 co‐ordinates are used (Zone 19).



4.2 Environmental Permits

Important components of environmental law (Ley 64‐00, 2000) are:

An environmental permit is not necessary to conduct geological mapping, stream sediment, sampling, line cutting or geophysical surveys.

A letter of no objection (Carta de no objección) from the Ministry of Environment is all that is required for trenching and initial drilling, as long as access routes need not be constructed. This letter is based on a brief technical description submitted by the company.

Additional drilling and the construction of any access roads warrant an environmental license that is valid for one year. A report must be filed by the company and must include technical and financial aspects that take into account remediation costs.

At the feasibility stage, an environmental impact study must be submitted and approved by the government.

Minera Camargo has not reviewed, nor has any opinion on the status of Everton Minera Dominicana’s environmental or social permits. Most of the drilling has been completed using low‐impact, man portable drills, and no significant land disturbance or pollution of any type was observed in the field. Most of the historic drill‐sites have been re‐vegetated, and the only evidence for the holes are field markers (cement caps, drill pipe etc.). Local workers have been involved in past exploration programs, and all of the people that the author talked to look forward to more work.

5.0 Accessibility, Climate, Local Resources, Infrastructure and Physiography The Dominican Republic has three major highways are DR‐1, DR‐2, and DR‐3, which go to the northern, southwestern, and eastern parts of the country, respectively. Access in the Property area is via a system of all‐weather country roads used by local cattle ranchers and farmers which branch off of Highway DR‐1. The Capital city of Santo Domingo is located about 140 kilometers to the south of the Property. Modern deep‐water port facilities are located near Santo Domingo, and Barrick Gold is currently upgrading Highway DR‐1 for the purpose of transporting materials to the Pueblo Viejo mine site. The nearest major population center is Cotuí (Fig. 4.1).

The majority of the country has access to electricity. Household and general electrical service is delivered at 110 volts alternating at 60 Hertz. However, electric power service has been unreliable since 1963, and as much as 75% of the power generating equipment is more than fifty years old. Some areas have power outages lasting as long as 20 hours a day. Many of the generating companies are undercapitalized and at times are unable to purchase adequate fuel supplies.

The Property is located in the eastern foothills of Cordillera Central at elevations ranging from 100 to just over 500 meters. The Yuna River flows northwest of the Property, and is dammed by the Hatillo Dam. The average annual temperature hovers around 25°C (77°F), and the average rainfall in the Property area is about 1850 mm per year. The Dominican Republic, like most of the Caribbean, is located in an area where hurricanes occur, mainly from the beginning of June to the end of November.

Major earthquakes occur on the island of Hispaniola about once every 50 years. Currently, there is a heightened earthquake risk on the Septentrional fault zone, which cuts through the highly populated region of the Cibao Valley north of the Project area. In addition, the geologically active offshore Puerto Rico and Hispaniola trenches are capable of producing earthquakes of magnitude 7.5 and higher. Earlier this year (12 January 2010), there was a magnitude 7.0 earthquake centered approximately 25 kilometers WSW from Port‐au‐Prince, Haiti at a depth of 13 kilometers on the Enriquillo‐Plantain Garden fault system which traverses the southern margin of the Dominican Republic. Refugees from Port‐au‐Prince have been migrating to the Dominican Republic since the date of the disaster.

The economic base of the Property area is mainly agriculture and cattle ranching. Vegetation mainly consists of crops and grasses. South of Cuance, submontane rain forest occurs in non‐cultivated areas. Crops include sugarcane, coffee, cocoa, tobacco, bananas, rice coconuts, cassava, tomatoes, pulses, dry beans, eggplants and peanuts. Mining is an increasingly important economic activity, and Barrick Gold’s Pueblo Viejo mine currently employs about 3500 workers.



6.0 History There are no significant historic mine workings or past mineral production on the Property. The largest known prospect is Spanish Pit in the Lechoza prospect area, a hole about 10 meters long and 4 meters wide dug into ferruginous gossan that may have been excavated in the 1800’s. The mineral potential of the Central Dominican Republic, particularly the Maimón Formation, was recognized by Bowin (1966); however, most systematic mineral exploration was done by multi‐national mining companies after Ley‐146 came into effect in 1974.

1977‐1979: Pan Ocean Minerals completed airborne magnetics, regional geochemistry and soil geochemistry. The program culminated in trenching and 3 shallow drill holes of La Lechoza as well as four diamond drill holes at Los Hojanchos. Elsewhere in the Belt, Falconbridge found and drilled the volcanogenic massive sulfide deposit at Cerro de Maimón in 1978.

1980’s: Rosario Dominicana completed soil geochemistry of Loma La Cuaba, airtrack drilling of Loma La Cuaba, and airtrack drilling of La Lechoza (1426 meters of drilling in 62 holes less than 48 meters deep). They also obtained the rights to explore the Maimón Formation and completed an airborne geophysical survey (magnetic and electromagnetic) and produced a 1:25,000 geologic map. Falconbridge conducted regional gossan sampling. The Mines Department collected soil samples and stream sediment samples and analyzed them for Au, Ag, Cu, Pb, and Zn. Very low frequency electromagnetic (VLF), magnetic, and time domain induced polarization (IP) surveys were completed on different prospects. At Cuance, Battle Mountain Gold completed mapping and rock sampling with negative results.

1996‐1998: Sysmin completed 1:50 000 scale geological mapping and stream sediment geochemical surveying for the Government. Geoterrex re‐interpreted the airborne geophysical data.

1998‐1999: On the Los Hojanchos concession, Falconbridge, then Corporación Minera Dominicana (CMD), completed 1:10,000 scale geologic mapping, sampling of road cuts and trenches (553 samples), a gridded soil survey, an IP survey (Warne et al., 1999), and a magnetic survey. Four trenches (997 meters) and four diamond drill holes (659.6 meters in LH‐01 to LH‐04) were also completed. At Cuance, CMD completed prospecting and sampling work.

2001: Falconbridge and Globestar recompiled the data, and re‐interpreted the 1983 airborne geophysical survey. CMD collected 171 rock samples at Cuance. Newmont Mining won the bid on the tender of the APV Fiscal Reserve, and completed data compilation, mapping and rock sampling. Newmont decided not to continue working on the APV concession.

2002: The APV Fiscal Reserve was converted to an exploration concession by presidential decree number 169/02 on 7 March 2002 and granted under special contract to Minera Mount Isa Panamá, S.A. (MIM) on March 25, 2002. MIM completed soil, rock and stream geochemistry and 154 meters of trenching. The trenching defined a major gold anomaly of 1.63 g/t Au across 154 m (Dominguez, 2008a).

2003: MIM completed ground IP and magnetic surveys at La Lechoza (10 line km in 5 lines at 300 meter spacing), Colorado (6 line kilometers in 2 lines at 250 meter spacing) and ground IP only at La Cuaba (12 km in 7 lines at 400 meter line spacing). They also completed soil and rock geochemistry in the different target areas. Based on the exploration results, they completed 1521.34 meters of diamond drilling in 8 holes at La Lechoza (LL1 to 8), and 235.55 meters of drilling in one hole at Colorado (La Cuaba). Everton entered into an option agreement with Globestar on 27 August 2003. The agreement allowed Everton to earn 50% of Globestar’s interest in the Los Hojanchos, Cuance, and Loma de Payabo concessions in return for exploration expenditures of US$390,000 per concession for a total of US$1,170,000 over a three year period. In December of 2003, Everton entered into an agreement to earn 50% of MIM’s interest in the Loma el Mate concession in return for exploration expenditures of US$500,000 over a two year period and payment of 100,000 shares upon signing followed by 50,000 shares and US$30,000 on the first anniversary followed by 50,000 shares and US$40,000 on the second anniversary.

2004: Everton completed a second round of 585 meters of drilling in six holes at Los Hojanchos (LH‐05 to 10). MIM changed its name to Linear Gold Caribe S.A. and completed soil geochemistry at La Lechoza as well as 1540.57 meters of drilling in six holes on Loma La Cuaba (APV04‐1,3,5,8, 10 and 12). Additional rock sampling was done at Cuance.

2005: Everton completed a regional stream sediment sample survey. CMD and Linear Gold completed two rounds of stream sediment sampling followed up by mapping and soil sampling of Loma El Mate. TMC Geophysics completed an IP



survey of Loma El Mate, which was followed up with 1334 meters of drilling in 13 holes. Linear Gold completed 1858 meters of drilling in 18 diamond drill holes at La Lechoza (LE holes).

2006: Everton Minera Dominicana completed 1378 meters of shallow airtrack drill holes on the Jobo Claro concession (JC‐01 to JC‐96, all less than 32 m deep. Mapping was completed in the Cuance River, and an additional 105 rock samples were collected. The soil grid on Loma El Mate was extended to the south, and 997 additional samples were collected to cover the Cuance prospect.

2007: Everton entered into an Agreement with Linear Gold whereby it can earn an undivided 50% interest in the APV Concession by making cash payments totaling US$700,000, performing minimum Work of US$2,500,000 and issuing 1,200,000 Everton common shares over a three‐year period. The Company can acquire a 65% interest in the concession by incurring all additional expenditures on the concession to the completion of a bankable feasibility study and by paying Linear US$2,000,000 and issuing 1,000,000 additional Everton common shares. Everton completed a helicopter borne geophysical survey on all of its active concessions in the Dominican Republic (Sharp, 2007). On the Jobo Claro concession it completed 22 line kilometers of Max‐Min ground electromagnetic surveys and 796 meters of diamond drilling in 4 holes (JCDH holes). On the APV concession, Everton completed 1:10 000 geological mapping, 3665 soil samples, 2229 rock samples and 201 meters of diamond drilling in two holes on the APV concession (APV holes, central area). At Cuance, 182 meters of hand‐trenching in the central portion of the soil anomaly were completed.

2008: 1003.6 meters of diamond drilling in 8 holes were completed at Cuance (Carrasco, 2008). Everton completed 177.9 meters of drilling in 2 holes at Loma El Mate (TBM 26 and 27). On the APV concession, 38 line kilometers of IP surveys were completed, and 1:5000 geological mapping was done of selected areas.

2009‐2010: Between 2009 and 2010, Everton completed 3665.76 meters of diamond drilling in 36 additional APV holes and a systematic alteration study of La Cuaba lithocaps.

7.0 Geological Setting

7.1 Regional Geology

The Dominican Republic and the Greater Antilles in general, are composed of fragments of intra‐oceanic island arc volcanic rocks. These fragments were probably once part of a single, continuous, southwest‐facing island arc that formed off the west coast of the Americas and was active from Lower Cretaceous through Eocene time (Nelson, 2004). In the Dominican Republic, the axial primitive island arc (PIA) is preserved in submarine to locally subaerial volcanic rocks of the Los Ranchos Formation. Coeval Lower Cretaceous bimodal volcaniclastic rocks of the fore‐arc basin are preserved in the Maimón and Amina Formations south and west of Los Ranchos. The Los Ranchos Formation is locally overlain by Albian reef limestones of the Hatillo Formation. These are in turn overlain by black argillites of the Lagunas Formation. Los Ranchos, Hatillo and Las Lagunas Formations are overthrust by the Maimón Formation. The Maimón Formation is overthrust by Lower Cretaceous Duarte peridotites which are overlain by submarine (MORB) basaltic rocks of the Upper Cretaceous Peralvillo Formation (Fig. 7.1). All of the Mesozoic rocks are cross‐cut and overlain by Late Cretaceous to Tertiary calc‐alkaline arc plutonic, volcanic and sedimentary rocks.



Fig. 7.1 Regional Geological Map of the Island of Hispaniola (Draper and Gutierrez‐Alonso, 1997)

7.2 Property Geology

7.2.1 Maimón Formation

The Maimón Formation, possibly the oldest stratigraphic unit in the concession area, outcrops in the southwestern corner of the Loma El Mate concession and underlies most of the Cuance and possibly Los Hojanchos concessions. It is bounded to the northeast by the Hatillo Thrust Fault and to the southwest by over thrust basalts of the Peralvillo Formation, forming a zone about 7.5 kilometers wide in the Project area. Based on geological mapping of the San Antonio concession, centered 12 kilometers southeast of Cuance, Holbek and Daubney (2000) define four lithostratigraphic units in the Maimón Formation. From the base upwards these are:

1. Lambedera Mafic Unit. This unit is more than 700 meters thick and consists of pillow basalts and basaltic andesite with variable amount of feldspar, interflow sediments (black argillite) and mafic‐derived volcaniclastic rocks. The upper contact is overlain by jasper horizons.

2. Parcela Rhyolite. This unit is about 500 meters thick and consists of rhyolite flows and lapilli to ash tuffs. The volcaniclastic rocks can be intercalated with minor volcanic rocks, jasper horizons and volcanogenic massive sulfides. Copper‐rich stock work zones also occur in these rocks.

3. Mosquito Argillite. These rocks are 100 meters to more than 900 meters thick and consist of thinly to medium bedded fine to coarse grained argillites, greywackes and occasionally jasper. Graded bedding, load casts and flame structures observed by Daubney and Holbeck (2000) imply that stratigraphy is upright, younging to the south.

4. Leonorita Schist. This is a section of bimodal volcanic rocks on the order of 800 meters thick. The mafic rocks consist of amygdaloidal flows, and they are intercalated with rhyolite crystal tuffs and inter‐flow sediments. In general, the grain size of these rocks is smaller than clastic rocks of the Parcela Rhyolite. The Leonorita schist is characterized by a strong penetrative deformation.

The Maimón Formation has been postulated as a mega shear zone resulting from the hot obduction of the Loma Caribe serpentinized peridotites as a north verging thrust block (Draper and others 1996). The resulting deformation varies in



intensity (Draper and Lewis 1991), but in general consists of a well‐defined planar fabric dipping moderately to the SW. Massive sulfide horizons in the Maimón Formation are easily deformed, and generally occur parallel to the regional foliation (F1), with a gentle plunge of about 25˚S (Lewis et al., 2000).

7.2.2 Los Ranchos Formation

Los Ranchos Formation represents the axial arc terrane, is penecontemporaneous with the Maimón Formation, and forms a 17 kilometer wide zone between the Hatillo Thrust and Tertiary limestone platform to the northeast. The Los Ranchos Formation was been mapped by Martín‐Fernández and Draper in 1998 as part of the SYSMIN mapping project. From the base upwards, Los Ranchos formation consists of 7 principal members:

1. Cotuí Basalt. This unit is more than 800 meters thick and consists of pillow basalts and basaltic andesite with variable amount of feldspar, interflow sediments (black argillite) and mafic‐derived volcaniclastic rocks. Drill holes at La Lechoza mainly intercept Cotuí basalt and intrusive rocks, as well as locally bedded volcanogenic massive sulfide.

2. Quita Sueño Dacite. This unit is about 600 meters thick and consists of quartz‐feldspar porphyritic dacite flows, agglomerates and ash‐flow tuffs with local sub‐volcanic sills, dikes and laccoliths. These rocks yield a U‐Pb age of 116.9 +/‐0.9 Ma (Kesler et al., 2005).

3. The Zambrana tonalite is centered under the Jobo Claro concession and appears to cover an area on the order of 9 kilometers long by 4.5 kilometers wide. These crystalline rocks have a U‐Pb age of 112.9 +/‐0.9 Ma (Kesler et al., 2005. Petrographic descriptions are limited to “a siliceous intrusive rock with a propylitic overprint” (sample 313228; Appendix 2). The largest drill hole intercept of tonalite occurs in Hole JCDH‐04 between 130 and 200 meters depth.

4. Meladito Lahar. The Meladito Formation is a fining‐upwards sequence of mud‐matrix supported blocks of rhyolite, tonalite and basalt at the base that grades upwards into fossiliferous sediments. This unit occurs south and west of the fossil volcanic edifice that might be currently marked by upper Cretaceous tonalites in the central part of the Jobo Claro concession. Holes JCDH‐03 and 04 intercepted thick sections of polymict volcanic breccia with clasts of basalt and tonalite up to 50 cm across.

5. Zambrana Dacitic Ignimbrite. This unit consists mainly of lapilli tuff, breccia and co‐genetic flow domes. The flow domes at Pueblo Viejo yield a U‐Pb age of 110.9 +/‐0.8 Ma (Kesler et al., 2005). These rocks are mineralized, and pervasively altered to dickite, kaolinite and other clay minerals (sample 25627; Appendix 1). Zambrana Ignimbrite is intercalated with minor andesitic volcanics (Platanal andesites??) west of Pueblo Viejo.

6. Pueblo Viejo (PV) Member. This unit consists of quartz crystal rich sediments and abundant black organic matter. It is the host rock to the volcanogenic massive sulphide protore of the giant Pueblo Viejo gold deposit (Photo 15.2). In the vicinity of the Monte Negro pit, the Pueblo Viejo Member is pervasively altered to dickite (sample 25618; Appendix 1). Kesler et al. (2005) report that the rocks contain fossil tree trunks and thin layers of coal. The Pueblo Viejo member is penecontemporaneous with the Zambrana Dacitic Ignimbrite and the OAE1 anoxic ocean event. All of these characteristics imply that the PV member was deposited in a shallow marine, restricted basin.

7. La Cuaba Schist (lithocap). West and south of Pueblo Viejo, the rocks are affected by pervasive pyrophyllite alteration and silica‐iron metasomatism. The alteration is so intense and pervasive that the origin of these schists is uncertain, but they are thought to be derived from hydrothermally altered Zambrana Dacitic Ignimbrite and penecontemporaneous Pueblo Viejo Member. Like the Zambrana ignimbrite, La Cuaba schist is locally intercalated with minor (less than 15%) porphyritic andesitic volcanic rocks.

7.2.3 Hatillo Formation

The Lower Albian Hatillo reef limestone conformably overlies the Los Ranchos Formation, and outcrops intermittently over a 10 kilometer long area between Piedra Imán and drill hole JCDH‐01, southwest of La Cuaba lithocap. Drill holes have intercepted more than 195 meters of Hatillo limestone, and the original depositional thickness might have been 400 to 1000 meters (Sillitoe, 2006). The basal 300 meters of the limestone are silicified and partly replaced by high grade magnetite and hematite ore. In the 1950’s, up to 700 000 tons of iron were mined from the Las Lagunas and Hatillo iron deposits on the southern and western sides of the Loma La Cuaba lithocap.



7.2.4 Las Lagunas Formation

The Las Lagunas Formation consists largely of fine grained, laminated, carbonaceous shales intercalated with epiclastic volcanic derived sediments and minor carbonates (Bowin 1966). This sequence is believed to represent a limited fore‐arc basin formed related to the overlapping Late Cretaceous to Early Tertiary arc. The rocks of the Las Lagunas formation are not known to contain any significant mineral occurrences although it is not uncommon to find intervals of syngenetic sulphides (pyrite) and locally anomalous Cu and Zn values (Domínguez, 2008).

7.2.5 Peralvillo Formation

Pyroxene andesite pillow lavas of the upper Cretaceous Peralvillo Formation outcrop about 9.5 kilometers southwest of the Cuance concession where they are overthrust onto felsic schists of the Maimón Formation. Trace element geochemistry indicates that the basalts are of mid‐ocean‐ridge affinity (Childe, 2000).

7.2.6 Late Cretaceous to Tertiary diorite/dacite intrusions

Undeformed mafic intrusions occur as laccoliths, sills, dikes, sub‐volcanic intrusions and extrusive basalts in and overlapping the Maimón and Los Ranchos Formations. The rocks consist of hornblende, plagioclase feldspar and variable amounts of magnetite. Drill holes APV09‐05, 06, 07 and 08 all intercept diorite. Diorite dikes and (possibly) cogenetic, partially emergent (supracrustal) basalts also occur in the Monte Negro (Photo 15.4) and Moore pits at the Pueblo Viejo gold mine. These rocks are related to development of a calc‐alkaline arc on top of the Early Cretaceous primitive island arc rocks. They are co‐eval with alunite in quartz veins from the Pueblo Viejo gold mine. Previous mappers had assigned these basalts to the Los Ranchos Formation, but some textures such as non‐metamorphosed “crumble breccias” might imply a younger age.



Fig. 7.2 Geological legend for maps in this report.



Fig. 7.3 Geological compilation map of the Property showing mineral prospects and payable diamond drill intercepts (red). Dashed red line shows La Cuaba lithocap. Solid red lines are open pit mines. Purple dashed line shows location of a magnetic high that may be related to a buried intrusion or magnetite body. Solid purple lines are areas of high vertical magnetic gradient where the intrusions might come closer to surface. The Maimón Formation outcrops

southwest of the Hatillo Thrust, and Los Ranchos Formation outcrops northwest of the thrust. Grey dots are traverses by the author.



8.0 Deposit Types Two ages of mineralization are thought to occur on the Property: (i) syn‐depositional volcanogenic massive sulphide (VMS) deposits of Upper Cretaceous age, and (ii) epigenetic gold vein deposits that are probably related to an unexposed Late Cretaceous or Tertiary porphyry copper‐gold system (such a porphyry might be centered below La Cuaba lithocap within or close to the magnetic high of Fig. 7.3). At Pueblo Viejo, these two ages of mineralization are juxtaposed in the same location (Photo 15.3). Elsewhere on the Property, VMS deposits hosted in the Maimón Formation occur at Cuance, Tres Bocas and probably Los Hojanchos. The origin of La Lechoza is uncertain (section 9.4), but it might be a VMS deposit in the Los Ranchos basalts modified by Late Cretaceous to Tertiary veining. Pueblo Viejo volcanogenic massive sulphide protore is interlaminated with carbonaceous rocks of Pueblo Viejo Member of the Los Ranchos Formation. The VMS deposits of the Maimón and Los Ranchos Formations tend to be copper and zinc rich with elevated precious metals and low lead values. The metal assemblage reflects the fact that they occur in primitive arc (PIA) rocks with low potassium and lead contents (Childe, 2000).

North‐westerly trending epithermal quartz veins in tension fractures cross‐cut the black shales and volcanic rocks, and the Pueblo Viejo mine is centered on this structural corridor. Ar‐Ar dating of alunite in some of these veins yields ages between 77 to 62 Ma, or Late Cretaceous to Early Tertiary (Kesler et al., 1981). This age is co‐eval with other diorite intrusion on Hispaniola.

8.1 Volcanogenic massive sulfide deposits

Volcanogenic massive sulfide (VMS) deposits share the following characteristics (Gifkins et al., 2005):

VMS deposits are hosted by submarine volcanic and sedimentary rocks.

They are the same age as the host rocks.

Most deposits are hosted in volcaniclastic units between major volcanic formations.

Economic parts of the deposits typically comprise more than 80% (massive) sulfide

Principal ore minerals are pyrite, sphalerite, galena, chalcopyrite and possibly pyrrhotite.

Stringer‐stockwork zones commonly underlie massive sulfides and may carry economic copper grades (Fig. 8.1).

Geochemically, most VMS deposits are characterized by Fe, Cu, Pb, Zn, Ag and sometimes Au and Ba.

Ore metals can be vertically zoned from iron and copper sulfides at the base of an ore lens through to lead and zinc sulfides on the periphery. Some ore lenses carry significant barite with or above the Pb‐Zn sulfides.

Massive sulfides can grade laterally into distal exhalites characterized by cryptocrystalline quartz, iron oxides, jasper, manganese oxide and elevated (but usually non‐economic) metal concentrations.

VMS deposits occur above extensive footwall alteration zones that form by hydrolysis of feldspar. Primary alteration minerals include sericite, quartz, pyrite, and chlorite. In systems with highly acid fluids, kaolinite, pyrophyllite and even dickite may occur. These minerals are zoned in a systematic fashion from zones of high fluid flux outwards into less‐altered host rocks (Fig 8.1). In metamorphosed VMS deposits, aluminous alteration minerals metamorphose to cordierite, andalusite, or kyanite.

The geometry of the footwall alteration zone depends on the competency of the host rocks. In sequences dominated by flows and domes, fluid flow is focused by sub‐vertical synvolcanic faults, and the alteration zones are pipe‐like. In contrast, stratabound alteration (mineralized) zones are more commonly developed in permeable rocks such as tuffs, breccias and sediments, particularly under impermeable cap‐rocks such as sills (Gifkins et al., 2005).



Figure 8.1 Essential characteristics of an idealized gold‐rich volcanogenic massive sulfide deposit. (Dubé et al, 2007). Note the position of chlorite alteration is

distal to the clay‐sericite alteration, which occurs in the footwall. In base metal (low sulfidation) VMS prospects, chlorite occurs in the proximal footwall.

8.2 Porphyry copper systems

Porphyry copper systems are defined as large volumes (10 to more than 100 km 3) of hydrothermally altered rock centered on intrusive stocks that may also contain skarn, carbonate‐replacement, sediment‐hosted and high sulfidation epithermal base and precious metal mineralization (Fig. 8.3; Sillitoe, 2010). The majority of the world’s porphyry systems occur in Tertiary calc‐alkaline batholiths and overlying volcanic chains. The deeper parts of porphyry Cu systems may contain porphyry Cu +/‐ Mo +/‐ Au deposits of up to 10 billion tonnes in size. Typical hypogene porphyry copper deposits have average grades of 0.5 to 1.5% Cu, <100 ppm to 400 ppm Mo and trace to 1.5 g/t Au. Large (disseminated) high‐sulfidation epithermal deposits average 1 to 3 g/t Au, but contain less copper than the underlying porphyry copper deposits.

Porphyry copper systems share the following characteristics (Sillitoe, 2010):

The main economic hypogene ore minerals are chalcopyrite, bornite, molybdenite, sphalerite, galena, native Au and electrum. Associated minerals include pyrite and magnetite.

Silicate alteration minerals include: quartz, biotite, K‐feldspar, actinolite, albite, tourmaline, dumortorite, muscovite, andalusite, pyrophyllite, alunite, clay minerals, epidote and chlorite.

They are spatially associated with porphyritic intrusions.

Porphyry copper systems are localized by deep, crustal‐scale faults which allow for rapid ascent of magmas and generation of a hydrothermal fluid.

The ore zones of hypogene porphyry copper deposits occur at paleo‐depths ranging from 1 to 5 kilometers.



Porphyry copper deposits are overlain by extensive lithocaps that may have an area of up to 100 km2 on surface. The vertical distance between the lithocap and potassic alteration related to the porphyry copper deposit ranges from 500 to 1000 meters. The lithocap itself might be as thick as 1000 meters.

Advanced argillic alteration preferentially occurs in rocks with a low acid‐buffering capacity such as rhyolite tuffs. It is less common in mafic rocks as these tend to neutralize acidic solutions.

Above the porphyry copper deposit, the lithocap may be enriched in As, Mo, Te, Bi, W, and Sn.

High sulfidation lode gold deposits can occur in the pyrophyllite zone at the base of the lithocap, and large disseminated high‐sulfidation gold deposits tend to occur in the quartz‐alunite zone above the pyrophyllite zone (Fig. 8.3).

Fig. 8.2 Essential characteristics of a porphyry copper system showing a centrally located porphyry Cu +/‐ Au +/‐ Mo deposit in a multiphase porphyry stock and its immediate host rocks. High‐sulfidation gold deposits can occur inside the lithocap environment (from Sillitoe, 2010).

Fig. 8.3. Generalized alteration‐mineralization zoning pattern for porphyry copper deposits (from Sillitoe, 2010).

8.3 Epithermal gold deposits

Most of the known economic epithermal precious metal deposits occur in Tertiary volcanic rocks, both in arcs and in post‐arc extensional settings. Important characteristics of epithermal deposits include:

High grades of Au and Ag.

Anomalous concentrations of Sb, As, Hg, Pb, Zn, Cu and other metals.

Ore minerals include native gold, electrum, acanthite, tetrahedrite, ruby silver, sphalerite, galena and chalcopyrite.

Mineral and metal zoning is significant from base metal‐rich roots to gold rich bonanza zones to silver‐rich zones above the bonanza zones.

Gangue minerals include quartz, calcite, barite, clay, sericite, chlorite and epidote.

Most known deposits are vetiform, but stockworks, breccias and disseminated deposits also occur.

They are associated with significant alteration zones (“color anomalies”) and lithocaps that are mainly related to condensation of magmatic vapor.



Exposure of ore zones is usually poor as the dominant dimension is down‐dip or down plunge of the ore shoot. The down‐dip extent of ore zones ranges from 200 meters on low sulfidation systems to more than 1200 meters in intermediate sulfidation systems.

Minerals are deposited in open spaces, and have characteristic textures (e.g. colloform banded and cockscomb textures are typical).

Alteration mineral assemblages indicate temperatures of deposition between 100 and 300ºC. Typical alteration types include: (i) proximal propylite, (ii) distal zones of clay alteration and (iii) unmineralized, but related zones of steam‐heated alteration or “lithocaps”.

Several sub‐classes of epithermal deposits are recognized: (i) low sulfidation, (ii) intermediate sulfidation and (iii) high sulfidation. Having said that, different classes of deposit may occur in the same camp, and some styles may overprint earlier styles. High sulfidation epithermal gold deposits tend to occur in the upper parts of porphyry copper systems.

9.0 Mineralization

9.1 Tres Bocas gold‐rich VMS prospect

Tres Bocas is a VMS prospect that occurs on the southern boundary of La Cueva concession with the Cuance concession approximately 8 km SE of the Pueblo Viejo mine. It has been drill‐tested with 3375 meters of drilling in 38 holes. Payable intercepts are polymetallic with significant precious metals, and are listed in Table 9.1. The best overall intercept was 1.7 g/t Au, 62 g/t Ag, 1.2% Cu and 6.9% Zn across 19.42 m in Hole TBM‐07, however, core recovery from this drill hole was poor.

On surface, the mineralized trend is defined by a zone of gossanous float and kaolinite‐altered subcrop approximately 800 meters long and up to 100 meters wide that trends northwesterly (Photo 9.1). Geochemical surveying shows that the surface trace of the mineralized horizon is perhaps best defined by anomalous gold‐in‐soil results > 200 ppb Au that coincide with linear, west‐northwest trending IP anomalies as defined by Lambert (2005). Copper‐in‐soil is also markedly anomalous in the gossan area, but copper is much more widely dispersed than gold.

Massive sulfides consisting mainly of sphalerite and chalcopyrite with pyrite occur in and above quartz‐sericite‐andalusite schist (samples 19668, 19738, Appendix 3). The occurrence of andalusite (Al2SiO5) is significant as it either (i) formed from fluids with temperatures in excess of 360˚C, or (ii) it formed by metamorphism of pyrophyllite (Al2Si4O10(OH)2) or dickite (Al2Si2O5(OH)4). In either case, it would typify the copper‐gold stockwork zone below gold‐rich massive sulfide as shown in Fig. 8.1. Chlorite‐sericite‐quartz schist seems to be peripheral to, or below, the payable mineralization associated with the andalusite schists. On surface, andalusite weathers to kaolinite (Al2Si2O5(OH)4; photo 9.1). Finally, the presence of andalusite defines Tres Bocas as a gold‐rich, high‐sulfidation VMS prospect rather than a low‐sulfidation or “classic” VMS prospect (Dubé et al., 2007).

Southeast of a late fault that appears to have about 110 meters of left‐lateral movement in this area, the surface trace of the Tres Bocas horizon could be marked by anomalous gold‐in soil geochemistry. Drill holes TB‐01 and TB‐04 successfully intercepted the horizon (Fig. 9.1), but drill holes TBM‐01, TBM‐10 and TBM‐20 were probably collared into the footwall. The mineralization consists of disseminated sulfide that might represent a Cu‐Au replacement horizon in permeable tuffs below a basaltic flow or sill (Fig. 9.1; e.g. Gifkins, 2005).

Table 9.1 Drill intercepts from Tres Bocas. HoleID FROM_m TO_m Interval_m* Ag_ppm Au_ppb Ba_ppm Cu_ppm Mo_ppm Pb_ppm S_pct Zn_ppm

TB‐01 12.19 16.76 4.57 7 191 80 12272 43 39 9 255

TB‐01 39.62 41.15 1.53 4 134 180 758 8 12 8 33600

TB‐02 46.18 47.24 1.06 3 138 180 758 8 20 7 34600

TB‐04 59.79 67.05 7.26 4 479 90 12729 21 8 11 758

TBM‐02 21.34 21.74 0.40 106 1295 <10 24700 41 0 0 13500

TBM‐03 2.00 8.00 6.00 1 1674 93 826 66 0 0 75

TBM‐07 20.20 39.62 19.42 62 1711 14 12353 23 484 9 68498



HoleID FROM_m TO_m Interval_m* Ag_ppm Au_ppb Ba_ppm Cu_ppm Mo_ppm Pb_ppm S_pct Zn_ppm

TBM‐12 42.67 47.24 4.57 120 1357 13 7484 67 1425 6 80495

TBM‐15 50.90 55.78 4.88 6 150 24 1515 7 467 10 5252

TBM‐19 42.67 47.24 4.57 4 115 93 678 12 0 5 8573

TBM‐23 40.84 47.85 7.01 19 438 76 1338 3 247 2 27781

TBM‐24 36.00 44.20 8.20 65 414 111 3193 31 1419 8 41977

TBM‐26 33.60 55.90 22.30 19 294 101 1859 17 801 4 30702

ppm = parts per million, ppb = parts per billion, pct = percent

*Intercepts are thought to be close to true width as they were largely drilled perpendicular to the orientation of the geological formations.

Fig. 9.1 Cross‐section through Tres Bocas, looking northwest. The zone intercepted in these holes might be a Cu‐Au alteration zone in permeable tuffs below a relatively impermeable basalt cap.

9.2 Cuance gold‐rich VMS prospect

Cuance is a gold‐rich VMS prospect that is well‐centered in the Cuance concession approximately 12 km SE of the Pueblo Viejo mine. It has been explored with 1003.6 meters of drilling in 8 holes in late 2007 and 2008 (Carrasco, 2008). Payable intercepts are polymetallic with significant precious metals, and are listed in Table 9.2. The best overall intercept was 1.1 g/t Au, 3 g/t Ag, 0.3% Cu and 2.0% Zn across 18.00 m in Hole CUA‐04.



On surface, mineralization occurs in a gossanous section of schistose rhyolite lapilli tuff (photo 9.3) about 150 meters thick that is locally intercalated with fine grained tuffaceous or argillaceous layers. Anomalous gold geochemistry in rock and soil samples defines an area about 700 meters long by 530 meters wide in this tuff layer. Part of the width (about 160 m) might reflect a structural repeat of the mineralization across a north‐northwesterly trending (growth?) fault.

Outside the mineralized zones, rhyolite tuff is characterized by pervasive sericite (illite) alteration. Within the mineralization, andalusite and phengite are important alteration products. The significance of andalusite is explained in Section 9.1. Phengite is an iron and magnesium bearing white mica (K2(Mg, Fe)2(Al, Fe)2Si8O20(OH)4) that is characteristic of the VMS environment (Jones et al., 2005). Phengite is differentiated from other micas by the position of the Al‐OH feature in SWIR spectra. In general, Na‐rich micas have the Al‐OH minima between 2190 and 2195 nm, normal potassic micas have this feature between 2200 and 2208 nm, and those of phengite occur between 2216 and 2228 nm (Jones et al., 2005). At Cuance, phengite was identified in surface samples 25637, 25638 and 25641 (Appendix 1) as well as several core samples (e.g. 167220, 227, 228 from CUA‐03 and 167262 from CUA‐04, Appendix 2).

A study of 15 polished thin sections of Cuance drill core samples show that the principal hypogene sulfides are pyrite, sphalerite, chalcopyrite, bornite and minor galena with supergene chalcocite and covellite. Bornite is an important copper mineral that is typical of gold‐rich VMS deposits.

Like Tres Bocas, Cuance is thought to represent a replacement VMS horizon in permeable tuffs below a basaltic flow or sill that dips moderately west‐southwest (Fig 9.2). While most of the drill holes have intercepted Cu‐Au stockwork mineralization or replacement horizons in lieu of massive sulfides, additional exploration drilling down‐dip (possibly west‐southwest) of the known intercepts might result in a new massive sulfide discovery.

Table 9.2 Drill intercepts from Cuance. HoleID FROM_m TO_m Interval_m* Ag_ppm Au_ppb Ba_ppm Cu_ppm Mo_ppm Pb_ppm S_pct Zn_ppm

CUA‐02 0.60 6.50 5.90 6 1703 540 8208 19 30 1 3021

CUA‐02 21.50 35.00 13.50 1 90 142 7484 13 8 4 495

CUA‐03 27.50 50.00 22.50 6 164 159 6005 8 257 2 1914

CUA‐04 41.00 59.00 18.00 3 1066 59 3242 13 359 4 20238

CUA‐04 125.00 137.00 12.00 1 297 53 4042 11 14 5 302

CUA‐05 35.00 36.50 1.50 4 57 40 9280 7 11 4 213

CUA‐06 35.00 42.50 7.50 2 464 60 2990 13 51 4 8006

CUA‐06 65.00 68.00 3.00 3 1017 65 959 11 2201 3 31450


*Intercepts are thought to be close to true width as they were largely drilled perpendicular to the orientation of the geological formations.



Fig. 9.2 Cross‐section through Cuance, looking north‐northwest. The zinc content of the mineralization appears to be increasing to the west (down‐dip) of the Formations and additional drilling west of CUA‐04 might intercept massive sulphides.

9.3 Los Hojanchos

Los Hojanchos is a VMS prospect that is well‐centered in the Hojanchos concession approximately 14 km SE of the Pueblo Viejo mine. Rocks in the footwall of the VMS‐style mineralization have been drill‐tested with 1245.22 meters of drilling in 10 holes. Payable intercepts are polymetallic with significant precious metals, and are listed in Table 9.3. The best known overall intercept was 1.6% Cu across 1.2 m in hole LH‐01. Intercepts from LH‐03 might be substantially better, but the copper values exceeded detection and were not re‐measured.

Historic drilling at Los Hojanchos is mainly localized in basaltic rocks with minor intercalated felsic tuffs. On surface, mineralization occurs in quartz vein‐stockwork zones with brick‐red boxwork after chalcopyrite and pyrite (Photo 9.6). Primary alteration minerals are weathered to kaolinite. The principal drill target was an IP anomaly that is co‐incident with moderately anomalous gold‐in‐soil geochemistry (15 to 120 ppb Au in soil). The IP was probably responding to this stockwork style of mineralization, and drill hole intercepts are mostly narrow with 8 of 9 intercepts less than 3 m wide (Table 9.3).

About 700 meters southwest of the historic drilling, near the upper contact of a 500 m thick section of rhyolite lapilli tuff, there is a southwesterly zoned Cu‐Zn anomaly in soil that is 2.1 kilometers long and 800 meters wide. To the northeast, Cu/(Cu+Zn) ratios approach 1, and this area defines the footwall stockwork to a potential VMS horizon. To the southwest, near the contact with overlying basalt flows, the soils are Zn‐rich, with Cu/(Cu+Zn) ratios less than 0.4. In this area (840 m west of Yam Pit; Photo 9.7), there are several rock samples with an average value of 0.9% Cu, 0.5% Zn, and



19 g/t Ag. This area could represent a weathered massive sulfide horizon under an impermeable basalt cap (Fig 9.3), a similar geological environment to Cuance and Tres Bocas.

Table 9.3 Drill intercepts from Los Hojanchos. HoleID FROM_m TO_m Interval_m* Ag_ppm Au_ppb Ba_ppm Cu_ppm Mo_ppm Pb_ppm S_pct Zn_ppm

LH‐01 94.30 95.50 1.20 1 50 0 15845 0 16 0 83

LH‐01 170.30 171.34 1.04 11 30 0 1069 0 334 0 27670

LH‐02 43.25 46.25 3.00 1 50 40 5930 20 9 5 56

LH‐03 84.20 85.65 1.45 97 6 48 1904 35 4 3 337

LH‐03 169.30 170.80 1.50 1 ‐5 10 >10000 23 4 5 86

LH‐03 55.50 57.00 1.50 4 5 ‐10 >10000 3 4 5 448

LH‐05 13.72 22.87 9.15 2 575 28 393 4 17 4 22

LH‐09 32.01 33.54 1.53 1 42 30 7540 25 3 5 2500

LH‐10 89.94 91.46 1.52 4 84 30 8370 16 5 10 245


*The true with is not that well known as most intercepts are probably veins



Fig. 9.3 Cross‐section through Los Hojanchos, looking northwest. Several high‐grade rock samples about 1 kilometer southwest of past drilling campaigns mark the surface expression of a potential new massive sulphide discovery (image left).

9.4 La Lechoza (VMS?)

La Lechoza is centered in the APV north concession about 6.3 km north‐northeast of the Pueblo Viejo mine. The prospect has been tested by 5602.42 meters of diamond drilling in 54 holes. There are 42 payable polymetallic intercepts with significant precious metals, and these are listed in Table 9.4. The best overall intercept was APV 09‐24 with 583 g/t Ag, 0.4 g/t Au and 0.2% Cu across 17 m.

Mineralization is hosted mainly in basaltic rocks of the Cotuí member of the Los Ranchos Formation that have been intruded by numerous felsic sills and dikes, as well as mafic dikes. The primary surface expression of mineralization at La Lechoza is well developed supergene gossan exposed at Pon Hill, Spanish Pit and North Hill (Photos 9.8 and 9.9). Trench LT‐11, cut across the gossan at North Hill, returned values of 6.6 g/t Au and 19 g/t Ag across 22 m. The high gold values on surface appear to be due to supergene enrichment in the gossan as underlying sulfide mineralization has lower gold grades. Together, the gossans in the central part of the Lechoza prospect define an area about 1600 meters long by 700 meters wide.

Sulfide zones of polymetallic mineralization at Lechoza are hosted in moderately dipping breccia zones of uncertain origin. The breccias can occur in felsic intrusive rocks (photo 9.11), and in amygdaloidal basalts (photo 9.12). Most of the breccias lack significant quartz (e.g. photos 9.11 and 9.12), so they don’t appear to be epithermal‐style breccias. In fact, the breccia matrix mainly consists of black mud and glass shards, and the larger rock fragments have cuspate, jigsaw‐fit textures that are diagnostic of hyaloclastite breccias (photo 9.12). Hyaloclastite forms when hot lavas are erupted onto the seafloor and quench‐fragment. Should the hot lavas and sub‐volcanic flows or sills intrude wet sediment, the resulting steam explosions cause quench fragmentation of the lavas (formation of hyaloclastite) and violent disruption of the host sediment due to steam explosions which results in the formation of peperite, a complex mixture of sediment, glass shards and cuspate hyaloclastite breccia fragments (McPhie et al., 1993). At La Lechoza, it appears that felsic sills and dikes related to early phases of the Zambrana tonalite intruded wet, unconsolidated interflow sediments. The same fractures that provide conduits for the intrusions can transport sulfur and metal bearing brine, which can then migrate laterally along the brecciated horizon (s) and deposit sulfide either in the breccias as pervasive replacements of volcanic glass/sediment mixes or as exhalations on the seafloor.

The best copper grades at La Lechoza occur in sulfide breccias under the leached cap where supergene copper minerals such as cuprite, chalcocite and native copper were re‐deposited near the base of oxidation along oxidized fractures as coatings on pyrite crystals and amygdules. Alteration minerals in the supergene zone are mainly montmorillonite, kaolinite‐smectite and halloysite, low temperature minerals that can form from the breakdown of illite in acid supergene fluids. At depth, chlorite and illite are more important, both in rhyolites and in basalts. These minerals are typical of the sub‐propylitic alteration assemblage of Hauff (2005). Locally, coarsely crystalline sphalerite‐chalcopyrite veins in chalcedonic quartz do occur (e.g. APV 10‐06 23.5 to 24.5 m). These veins might be related to later Cretaceous or Tertiary epithermal style mineralization.

Finally, based on the core reviewed by the author, the origin of La Lechoza was just not very obvious. However, a photograph of bedded massive sulfide intercepted in Hole LL‐02 was published in a memo dated 29 February 2002 by Philip Pyle, V.P. Exploration for Linear Gold. Therefore, based on the occurrence of (i) hyaloclastite which indicates a submarine geological environment, (ii) bedded massive sulfides, and (iii) a moderately dipping, stratabound (?) geometry, it is the author’s opinion that the VMS model will be most helpful in guiding further exploration of La Lechoza. Having said that, Everton geologists have pointed out that there may be significant structural control to the deposit. It is not yet known if these structures are (ii) syn‐mineral faults as would be expected in the volcanogenic environment, or (ii) later Cretaceous‐Tertiary structures. If they are later structures, they may introduce additional gold to the VMS system at La Lechoza in the same way that they appear to have done at Pueblo Viejo.

Table 9.4 Drill intercepts from La Lechoza. HoleID FROM_m TO_m Interval_m* Ag_ppm Au_ppb Ba_ppm Cu_ppm Mo_ppm Pb_ppm S_pct Zn_ppm

APV09‐11 42.00 45.00 3.00 7 259 7 3336 12 0 8 2528

APV09‐13 20.35 45.50 25.15 1 155 23 355 2 0 3 8248

APV09‐15 10.00 14.50 4.50 1 427 112 3396 2 0 0 2261



HoleID FROM_m TO_m Interval_m* Ag_ppm Au_ppb Ba_ppm Cu_ppm Mo_ppm Pb_ppm S_pct Zn_ppm

APV09‐15 23.95 29.50 5.55 0 8 7 4324 4 0 6 196

APV09‐17 28.15 38.00 9.85 2 109 42 5802 9 0 5 1437

APV09‐19 6.50 18.50 12.00 7 307 1535 578 2 0 0 7190

APV09‐20 7.80 10.50 2.70 2 217 159 956 16 0 0 5004

APV09‐21 16.00 32.00 16.00 1 52 25 6629 1 0 2 1100

APV09‐22 32.00 52.50 20.50 0 15 10 13355 5 0 6 103

APV09‐24 0.00 17.00 17.00 583 421 205 2311 47 0 0 43

APV09‐24 98.00 99.50 1.50 5 183 18 5390 69 0 9 869

APV10‐01 0.00 38.00 38.00 37 475 640 1293 33 0 0 68

APV10‐02 0.00 9.50 9.50 2 284 95 3345 8 0 0 329

APV10‐02 18.50 44.50 26.00 2 166 32 8008 22 0 9 627

APV10‐03 35.25 44.00 8.75 5 169 22 8590 6 0 8 244

APV10‐03 10.00 19.00 9.00 52 3386 181 6266 67 0 0 627

APV10‐05 26.50 53.00 26.50 1 44 13 7068 19 0 9 180

APV10‐06 8.35 28.50 20.15 16 430 75 6360 65 0 2 15340

APV10‐06 40.50 45.50 5.00 10 92 15 3768 68 0 3 6817

APV10‐07 5.00 26.00 21.00 48 560 155 8621 94 0 4 8074

APV10‐08 1.80 7.50 5.70 13 656 252 2074 41 0 0 1427

APV10‐09 12.90 38.00 25.10 4 219 158 6368 2 0 2 854

LE‐01 0.00 10.00 10.00 1 1248 12 2256 60 0 0 145

LE‐01 18.00 40.00 22.00 1 83 17 4689 21 0 8 549

LE‐02 0.00 2.00 2.00 1 1825 90 1650 51 0 0 505

LE‐02 26.00 34.00 8.00 1 33 68 7788 3 0 3 641

LE‐03 24.00 56.00 32.00 0 63 14 7513 11 0 7 292

LE‐04 18.00 42.00 24.00 0 37 12 6533 14 0 9 155

LE‐05 16.00 22.00 6.00 5 135 30 10060 9 0 6 310

LE‐06 14.00 44.00 30.00 3 105 24 3453 8 0 8 509

LE‐07 18.00 32.00 14.00 1 113 10 12256 16 0 10 91

LE‐08 19.80 34.00 14.20 8 495 11 14677 15 0 8 1839

LE‐10 10.00 22.00 12.00 3 131 113 1929 4 0 1 2677

LE‐12 108.00 112.00 4.00 6 7 10 9050 13 0 1 1768

LE‐14 0.00 14.00 14.00 13 869 167 3301 13 0 0 1147

LE‐17 0.00 4.00 4.00 7 318 125 5040 3 0 0 823

LL‐01 4.00 28.00 24.00 2 14 453 2300 5 0 0 794

LL‐02 3.50 24.00 20.50 4 703 805 4595 22 0 4 819

LL‐03a 12.80 21.34 8.54 7 1524 2379 753 25 0 0 291

LL‐03b 8.00 38.00 30.00 8 1290 665 2414 10 0 1 962

LL‐04 8.00 40.00 32.00 2 281 571 15402 16 0 1 722

LL‐07 26.60 32.00 5.40 12 301 24 2930 36 0 5 41593


*The true width of the intercepts perhaps an average of 80% of the interval width.



Fig. 9.4 Cross‐section through La Lechoza, North Hill, looking northwest.

9.5 La Cuaba Lithocap

La Cuaba lithocap is about 11 kilometers long and 3.3 kilometers wide, with a surface area of about 33 km2. Geochemically, the lithocap is characterized by a strong Mo‐Te‐As anomaly in soil and rock samples, with local but potentially significant gold anomalies in soil and rocks (Fig. 10.5). The Pueblo Viejo gold‐zinc mine occurs in the eastern third of this alteration zone. The entire southern portion of the APV concession (west of Pueblo Viejo) is underlain by the lithocap, which has been tested by 2618.12 meters of diamond drilling in 11 holes. The only potentially economic intercept was APV 04‐12 with 0.9% Cu across 10 m. There are three other intercepts with anomalous, but sub‐economic gold and minor copper values (Table 9.5).

The geology of Loma la Cuaba very difficult to map due to the intense, rock destructive alteration. From the drilling, some volcanic textures are apparent in core that imply that the geology is mainly felsic lapilli and ash tuff intercalated with minor andesitic flows (or possibly finely crystalline diorite sills) ranging from 20 to 110 meters thick. The tuffs are pervasively altered to pyrophyllite and other clay minerals (Fig. 9.5). In the southwestern part of the APV concession, there is a zone of silica‐hematite‐pyrite alteration about 300 meters thick at the upper contact of the tuffs with the Hatillo limestone. About half of the drill holes intercepted smaller horizons of barren quartz‐pyrite‐specularite rock on the order of 10 to 70 meters thick that are hosted in the metamorphosed tuffs, and may replace either: (i) smaller intercalated limestone horizons, or (ii) permeable tuff horizons.

The lithocap is centered on a strong magnetic anomaly that might be related to (i) an intrusive complex at depth at depth, or (ii) magnetite deposit (with or without gold and copper). The intrusion is more than 300 meters deep based on:



(i) the fact that no drill holes have yet intercepted significant intrusive rocks and (ii) the pyrophyllite zone of the lithocap must have been positioned above the causative intrusion. Our interpretation of the geological and geophysical evidence suggests that the top of the main body of the intrusion is about 1.5 kilometers below surface. Variations in the magnetic field imply that smaller, younger intrusions or magnetite‐rich (potassic?) zones could come within 200 meters of surface.

Table 9.5 Drill intercepts from La Cuaba. HoleID FROM_m TO_m Interval_m* Zn_ppm Ag_ppm Au_ppb Ba_ppm Cu_ppm Mo_ppm Pb_ppm S_pct

APV04‐12 42.0 52.0 10 20 0 46 18 9084 46 0 6

APV04‐12 168.0 174.0 6 11 0 563 63 124 90 0 1

APV09‐02 149.0 158.0 9 22 0 132 6 1440 3 0 5

APV09‐03 17.0 56.0 39 72 1 267 56 1368 41 0 3


*The true width of these intercepts is not known as drilling is widely spaced

Fig. 9.5 Cross‐section through La Cuaba, looking northwest. Hole APV04‐12 intercepted 0.91% Cu across 10 m, and lower grade gold intercepts do occur in other holes in the lithocap (above the orange line). These intercepts might be related to veins (???—dashed red lines). This diagram, although hypothetical in many respects, does imply that gold mineralization might occur at or close to the transition between sericitic alteration and pyrophyllite‐dominant advanced argillic alteration. The location and dip of the porphyry is inferred from the magnetic survey data.



Photo 9.1. TRES BOCAS. Rare surface outcrop of quartz‐kaolinite schist in the footwall to the Tres Bocas massive sulfide. Check sample 25629, cut across the foliation of 170˚/65˚, yielded results of 361.4 ppm Cu and 206.7 ppb Au across 1.3 m. This sample is located 140 meters northwest of TBM‐07.

Photo 9.2. TRES BOCAS. Photograph of banded massive sulfide from TBM‐07, 28.96‐30.78 m. Sample 19661 yielded results of 281 g/t Ag, 4.9 g/t Au, 1.6% Cu, 12.3% Zn and 0.1% Pb across 1.82 m.

Photo 9.3. CUANCE. Rhyolite lapilli tuff in the hanging wall to the Cuance VMS prospect. Sample 25635 contains anomalous, but non‐economic values of 531 ppm Cu and 163 ppm Zn and the alteration mineralogy is mainly sericite (illite).

Photo 9.4 CUANCE. View of the Cuance VMS horizon where it outcrops next to the samplers. Sample 25637 contains 3.9 g/t Au, 26 g/t Ag, 0.5% Pb and 0.8% Zn across 2 m and the alteration mineralogy is mainly phengite (Fe‐Mg sericite). The bedding of the rocks in the foreground is 160˚/28˚ SW

Photo 9.5 CUANCE. Sample 167239 from CUA‐03 contains 1% Cu, 0.5 g/t Au, 5.6 g/t Ag and 0.2% Zn across 1.5 m (47‐48.5m). Mineralization consists of moderately crystalline pyrite and chalcopyrite in a siliceous matrix, and is typical of the stockwork zone below or adjacent to gold‐rich massive sulfide deposits.

Photo 9.6. CUANCE. Photomicrograph of sample 167282 from drill hole CUA‐04 (45.5 to 47 m). This sample contains 3.4% Zn, 0.1% Cu, 0.2 g/t Au across 1.5m



Photo 9.6. LOS HOJANCHOS. Quartz veinlets with red Fe‐oxide in schistose rhyolite lapilli tuff southwest of the historic drilling. Select sample 25632 from the veinlets contains 1047 ppm Cu and 18 ppb Au across 0.05 m.

Photo 9.7. LOS HOJANCHOS. YAM PIT – site of Pan Ocean DDH. A vertical sample cut across the oxidized rhyolite lapilli tuff yielded results of 876 ppm Cu and 967 ppm Zn across 2 m (sample 25642). The sample is probably very close to a VMS deposit.

Photo 9.8 LA LECHOZA. Ferruginous gossan at Spanish Pit. A grab sample from this outcrop contains 3174 ppm Cu and 587 ppb Au (sample 25612).

Photo 9.9 LA LECHOZA. Ferruginous gossan at North Hill. Sample 25617 yielded a result of 457 ppm Cu, 132 ppm Pb, 256 ppm Zn, 12 g/t Ag and 0.9 g/t Au across 3 m.

Photo 9.10 LA LECHOZA. Sample 311079 from APV 10‐02 contains 1.4% Cu and 0.4 g/t Au across 1 m (29‐30 m). The mineralization is hosted in a monzodiorite porphyry breccia in a matrix of sticky grey clay (mud??) with almost 85% finely crystalline pyrite.

Photo 9.11 LA LECHOZA. Sample 311516 from APV 10‐07 contains 0.3% Zn and 0.2 g/t Au across 1.4 m (23.1‐24.5 m). The mineralization is hosted in a basaltic hyaloclastite breccia with jigsaw‐fit amygdaloidal fragments in a pyritic mud matrix.



Photo 9.12 LA LECHOZA. Photomicrograph of sample 311268, APV 10‐03, 35.25‐35.6 m. This sample contains 0.3% Cu, 0.2 g/t Au across 1.25 m, and consists of monzodiorite porphyry breccia with chalcanthite stained feldspar and chalcocite coated pyrite. The matrix consists of clay and small fragments, but not quartz.

Photo 9.13 LA LECHOZA. Photomicrograph of sample 313262, APV 09‐15, 70‐71.2 m. This sample contains 6.4% Zn, 0.3% Cu, 0.3 g/t Au and 10 g/t Ag across 1.2 m. The mineralization occurs in blackjack sphalerite veins with pyritic selvedges in chlorite‐altered basalt. No hydrothermal quartz was observed.

Photo 9.14 LA CUABA. Silica and goethite matrix breccia, probably from weathering of magnetite. Sample 25625 contains non‐anomalous metal values.

Photo 9.15 LA CUABA. Sample 36243, APV 04‐08, 176‐178 m. This sample contains 71.5 ppm Cu and 22 ppb Au across 2 m. The core consists of finely crystalline pyrite and chalcedonic quartz with a specularite overprint.

10.0 Exploration

10.1 Airborne Geophysical Surveys

Between 29 January and 4 April 2007, Fugro Airborne Surveys conducted a HeliGEOTEM II (time‐domain) electromagnetic and magnetic survey of the Property on behalf of Everton Resources Inc. Using Santo Domingo and Bonao as a base of operations, a total of 2192 line kilometers of data were collected using an AS‐350 B3 helicopter. Line spacing was 100 meters, and tie lines were spaced every 1000 meters. The geophysical survey equipment used was: (i) a Scintrex Cs‐2 single cell cesium vapor magnetometer, (ii) a HeliGEOTEM 20 channel multicoil electromagnetic transmitter, and (iii) a multicoil receiver. The magnetometer sensor height was 72 meters above ground, the transmitter was 40 m above ground, and the EM receiver was 67 m above ground. Further details of the survey specifications and parameters are in Fugro’s Logistics and Processing Reports (Job No. 06302, 2007).

The survey data were processed and compiled in the Fugro Airborne Surveys Ottawa office. The collected and processed data are presented on color or black and white maps. The following maps were produced: (i) total magnetic intensity (TMI), (ii) Magnetic vertical derivative of TMI, (iii) Reduction to the Pole of TMI, (iv) Amplitude of dB/dt Z channel 6, (v) Amplitude of dB/dt Z channel 9 (vi) Amplitude of dB/dt Z channel 12, and (vii) flight path. In addition, digital archives of the raw and processed survey data were delivered to Everton Resources.



The magnetic survey has identified several features of interest to mineral exploration. Centered in La Cuaba lithocap, there is a strong positive magnetic feature that is about 5 kilometers long and 3.5 kilometers wide (Fig. 10.1). This area has been drill‐tested to a depth of 300 meters, and rocks in the drill holes are mainly rhyolite lapilli tuffs, pyrophyllite schist, quartz‐hematite‐pyrite rock and intercalated mafic volcanic flows. None of these rocktypes are particularly magnetic (see magnetic susceptibility measurements in Appendix 2), so the anomaly could be caused by either: (i) a buried intrusive complex more than 300 meters deep, or (ii) a massive magnetite orebody, also more than 300 meters deep. Variations in the magnetic field, best shown in the vertical gradient map, might highlight areas of complexity that could be related to different phases of an intrusive complex, or magnetite‐rich mineralization. Southwest of the Hatillo thrust, the magnetic survey shows a well‐defined northwest trending fabric that parallels the regional foliation of the Maimón schist. Within this zone, there are small magnetic highs between Lambedera and Los Hojanchos that might reflect QFP flow‐domes or intrusions in the schist. These might drive hydrothermal cells related to massive sulfide mineralization. Finally, the magnetically active corridor between La Lechoza (just northeast of the mineralization) and La Cueva co‐incides with mapped areas of the Zambrana Tonalite.

The electromagnetic survey was interpreted by Sharp (2007), and several potential bedrock conductors were identified. These are shown as orange squares on Figure 10.2. None of these co‐incide with known mineralization from drilling. The dataset was re‐processed and interpreted by Paterson, Grant and Watson (PGW) consulting geophysicists (Paterson et al., 2007). Processing and interpretation included computation of RTP, analytical signal, first and second derivatives of the magnetic data and construction of a DTM from the elevation data acquired. The processing included also micro‐leveling of the off‐time EMZ (dB/dt) for the channels 6 and 9 and the B‐field for channels 9 and 12 of the EM data, computation of the τ (TAU) time decay constant, and creation of Conductivity Depth Images (CDI) from Z dB/dt off‐time data using EMFlow™ processing software. Finally an interpretation map was compiled showing anomalies as possible conductors and qualifying these as weak, moderate, strong or artifacts, possible airborne IP effects, and conductive zones. Products were delivered both as geotiff images and hard copy printed in maps. None of the geophysical targets identified by PGW coincided with known mineralization either.



Fig.10.1 Gridded airborne magnetic data (TMI reduced to the pole; Fugro, 2007) showing, mineral prospects, and payable diamond drill intercepts (red). Dashed red line shows La Cuaba lithocap. Solid red lines are open pit mines. Purple dashed line shows location of a magnetic high that may be related to a buried intrusion. Solid purple lines show areas where the vertical magnetic gradient is large, and these might be shallower parts of an intrusive complex, or

areas of magnetite‐rich mineralization.



Fig.10.2 Map of amplitude of dB/dt Z channel 9 showing conductive areas in red, and resistive areas in blue. Mineral prospects, and payable diamond drill intercepts (red) are shown. Dashed red line shows La Cuaba lithocap. Solid red lines are open pit mines. Purple dashed line shows location of a magnetic high that may be related to a buried intrusion. Anomalous electromagnetic responses picked by Sharp (2007) as potential bedrock conductors are shown as

orange squares.



10.2 Soil Geochemistry

About 33% of the Property has been covered by soil sample grids in different exploration campaigns between 1999 and 2009, mostly according to the methods described in Section 12.1. The most recent work was 90% complete coverage of the APV II concession by Everton at 100 meter by 100 meter spacing over all but the northernmost part of the Property where samples were collected on a 200m by 200 m grid in 2008 and 2009. At Jobo Claro, 550 Ha were covered by soil samples at 100 meter by 100 meter spacing, also by Everton. Between Loma El Mate, Los Hojanchos and Cuance, an area of 1145 Ha is covered by lines 100 or 200 meters apart, with a sample spacing of 50 meters. Most of these samples were collected by the previous owners of these concessions. In selected areas, additional samples were collected at tighter spacing to better define geochemical anomalies. Collectively, an area of about 5340 Ha on the 16185 Ha Property has been covered by systematic soil sample surveys. All of the samples were analyzed for gold and base metals according to the methods of Section 13.1.

The author of this Report compiled all the soil geochemical analyses, and analyzed the distributions of Au, Ba, Mo, Pb and Zn. Ordinary distribution statistics are summarized in Table 10.1. The data for each element were then plotted as histograms, box‐and‐whisker plots, stem‐and‐leaf plots and probability plots. Each plot was interpreted, and thresholds for non‐anomalous (background), probably anomalous, and anomalous metal concentrations were determined (also summarized in Table 10.1). Of these elements, Au, Cu and Zn are the principal elements of economic interest on the Property. The data for these metals were gridded using Encom Discover’s inverse distance weighting algorithm, and contoured using the anomaly thresholds of Table 10.1. Results of this analysis show that the most important polymetallic soil anomaly occurs between Cuance, Loma El Mate and Los Hojanchos (Fig. 10.3). A smaller polymetallic anomaly defines La Lechoza (Fig. 10.4).

Table 10.1 Summary distribution statistics for 8576 soil samples. Au_ppb Ba_ppm Cu_ppm Mo_ppm Pb_ppm Zn_ppm

Maximum 6,340 2,320 9,630 153 687 6,445

Arithmetic Mean 10 53 66 2 8 85

Standard Deviation 91 79 150 6 19 172

50th percentile 3 29 39 0.6 4 54

75th percentile 6 60 78 1 9 96

90th percentile 16 130 130 3 16 167

95th percentile 35 190 201 6 23 254

98th percentile 76 264 354 13 42 452

ANOMALY THRESHOLDS

Non‐anomalous 0 to 28 0 to 135 0 to 130 0 to 3 0 to 16 0 to 230

Probably anomalous 28 to 152 135 to 430 130 to 330 3 to 15 16 to 42 230 to 453

Anomalous 152 to 6341 430 to 2321 330 to 9631 15 to 154 42 to 687 453 to 6445

ppm = parts per million, ppb = parts per billion



Fig. 10.3 Soil anomaly map for Loma El Mate, Los Hojanchos and Cuance. YELLOW=Au in soil >28 ppb, BROWN=Zn in soil > 230 ppm and CYAN=Cu in soil >130 ppm. Red dots are payable diamond drill intercepts. At Cuance, the Au‐Zn‐Cu anomaly is almost perfectly co‐incident with some zoning of zinc up‐section. Metal zoning is more apparent at the southern part of the Los Hojanchos anomaly where strong copper values in soil grades up‐section into Zn‐rich soil. At Tres Bocas, drilling below a strong Zn‐in‐soil anomaly led to the discovery of massive sulfide.



Fig. 10.4 Soil anomaly map for La Lechoza. YELLOW=Au in soil >28 ppb, BROWN=Zn in soil > 230 ppm and CYAN=Cu in soil >130 ppm. Red dots are payable diamond drill intercepts.

10.3 Rock Geochemistry

About 40% of the Property has been covered by reasonably detailed prospecting and rock sampling. The most recent work was 80% complete coverage of the APV II concession by Everton. All of the samples were analyzed for gold and base metals according to the methods of Section 13.2. Because the surface rocks are subjected to tropical weathering, and sulfides do not survive well in this environment, the anomaly thresholds for the rocks were determined in the same way as they were for the soil samples, rather than using economic thresholds. Specifically, the author of this Report compiled all the rock geochemical analyses, and analyzed the distributions of Ag, Au, Ba, Mo, Pb and Zn. Ordinary distribution statistics are summarized in Table 10.2. The data for each element were then plotted as histograms, box‐and‐whisker plots, stem‐and‐leaf plots and probability plots. Each plot was interpreted, and thresholds for non‐anomalous (background), probably anomalous, and anomalous metal concentrations were determined (also summarized in Table 10.2). Of these elements, Au, Cu and Zn are the principal elements of economic interest on the Property. The data are not plotted in this Report as they mainly highlight the same anomalies as the soil maps of Figures 10.3 and 10.4.



Table 10.2 Summary distribution statistics for 3974 rock samples. Ag_ppm Au_ppb Ba_ ppm Cu_ppm Mo_ ppm Pb_ ppm Zn_ ppm

Maximum 1,355 22,400 2,990 78,800 1,255 7,008 17,900

Arithmetic Mean 1 152 81 317 11 31 153

Standard Deviation 28 963 251 1,949 36 155 579

50th percentile 0 3 20 49 2 7 43

75th percentile 0 29 54 200 9 20 118

90th percentile 1 194 140 632 25 59 298

95th percentile 2 538 286 1,195 49 120 578

98th percentile 7 1,451 860 2,141 84 231 1,177

ANOMALY THRESHOLDS

Non‐anomalous 0 to 6 0 to 229 0 to 130 0 to 500 0 to 40 0 to 369 0 to 640

Probably anomalous 6 to 72 229 to 1129 130 to 470 200 to 2000 40 to 81 369 to 986 640 to 2100

Anomalous 72 to 1355 1129 to 22400 470 to 2990 2000 to 78800 81 to 1255 986 to 7008 2100 to 17900

10.4 Lithocap Alteration Study using a PIMA SWIR spectrometer

Reflectance spectroscopy is a technique that uses the energy in the Short Wave Infra‐Red (1.0‐2.5 microns) wavelength region of the electromagnetic spectrum to identify and analyse minerals (Hauff, 2005). The technique is especially useful for finely crystalline minerals that cannot easily be identified by visual inspection or even more sophisticated techniques such as X‐ray diffraction. Alteration mineral maps can be compared to models of known deposits (e.g. Figs. 8.2 and 8.4) to estimate the position of the sample in a hydrothermal system. Based on this information, the depth of drill targets in the mineralized system can be estimated.

In 2010, Everton Minera Dominicana collected 1995 surface rock samples from the southern part of the APV concession, mainly from stream drainages where there is clean rock exposure. The rocks were transported to the core shack at Cotuí, then dried in the sun and scanned with a PIMA reflectance SWIR spectrometer. Similarly, 669 core samples from drill holes in the lithocap were also scanned (mainly 2004 APV holes). The spectra were then examined by a trained operator, and the minerals were identified by comparing the sample spectra to reference spectra. Sometimes there are several different minerals in a sample, and the spectrometer comes with some software that allows the operator to “unmix” the sample curves. In practice, two or three minerals that might result in a sample curve can be resolved.

The data (mineral determinations) were delivered to the author of this Report 19 July 2010. After inspecting the information, it was decided to classify the mineral assemblages according to the criteria of Table 10.3. The mineral assemblages were plotted, and boundaries drawn as shown in Fig. 10.5. The map shows that more than 65 percent of the lithocap is characterized by advanced argillic alteration. Similarly, drill holes with SWIR spectra show that the alteration mineralogy is overwhelmingly dominated by pyrophyllite (advanced argillic assemblage 2) to a depth of more than 300 meters from surface. Based on the surface distribution of pyrophyllite, and the fact that all of the diamond drill holes bottomed in pyrophyllite, it appears that the true thickness of advanced argillic alteration in the lithocaps is about 1000 meters (Fig. 10.6). Rock samples from both surface and core contain minor, if any, gold or base metals. This is in contrast to samples collected from the Monte Negro pit which are dominated by sericite alteration. Specifically, of 10 samples collected from the Monte Negro gold mine, 8 were characterized as having illite alteration, and only 2 had pyrophyllite.

In porphyry systems, HCl forms a weak acid at high temperatures. Such a fluid is stable with respect to muscovite and sericite. As the fluid migrates upwards from the intrusive center and cools, HCl forms a strong acid that reacts with feldspar in the rock to form pyrophyllite. The reaction releases silica to the hydrothermal fluid, which appears to have migrated up‐section and ponded below the Hatillo Formation limestone where it replaced more than 75% of the limestone with finely crystalline chalcedonic silica, specularite, magnetite and pyrite (Fig. 10.6).

Gold precipitation from the hydrothermal fluid might be caused by cooling, a pH change, a change in oxygen fugacity or by boiling. Given that known gold mineralization at Monte Negro is associated with sericite alteration, and barren pyrophyllite alteration occurs above sericite (up‐section), it appears that the transition between these two alteration



styles marks the position of the thermodynamic boundary where gold precipitation occurred (Fig. 10.6). Furthermore, any open faults or structures at these levels would have enhanced gold grade potential as these areas of lower pressure would encourage boiling (possible lodes of Fig. 10.6).

Table 10.3. Mineral assemblages and interpretation summary.

Mineral Assemblage Interpretation*

Sericitic (phyllic): Illite or muscovite present but not smectite Alkali exchange with rock and near‐neutral fluid at temperatures hotter than 300ºC.

Advanced Argillic 3: Topaz and pyrophyllite Alkali stripping of rock with acidic fluid at temperatures between 250º and 300ºC.

Advanced Argillic 2: Pyrophyllite Alkali stripping of rock with acidic fluid at temperatures lower than 250ºC

Advanced Argillic 1: Alunite, Dickite Alkali stripping of rock with strongly acidic fluid at temperatures lower than 250ºC.

Argillic: Halloysite and/or Kaolinite These minerals form from moderately acid, low temperature solutions, and might form from acid solutions generated by pyrite in the near‐surface weathering environment.

Sub‐propylitic: Smectite (beidellite) and/or calcite present Volatile addition (mainly CO2 and H2O) to the rock.

Silicic: Quartz The identification of quartz alone is not diagnostic, and rocks with only “silicic” alteration were not mapped on Fig.10.5. For the information to be useful, something about how the quartz occurs has to be known (e.g. as cockscomb veins or pervasive silica replacement of pre‐existing rock??)

*Based on Hauf (2005) and Hedenquist and White (2005).



Fig. 10.5. Alteration Map with gold geochemistry for rock and soil samples shown. DASHED PURPLE = magnetic anomaly, SOLID PURPLE = area of high

magnetic vertical gradient, SOLID RED = open pit gold mines. Geological mapping under the alteration map is explained in the Legend of Fig. 7.2.



Fig. 10.6. Cross‐section through La Cuaba Lithocap and drill hole APV 04‐08. Dashed orange line is the contact between deeper sericite alteration and overlying advanced argillic alteration (pyrophyllite schist). Geological mapping is explained in the Legend of Fig. 7.2.

11.0 Drilling

11.1 Percussion Drilling

Some of the earliest exploration done on the Property was done using an airtrack drill. In the archives, there are records from Rosario Minera Dominicana for 1426 meters of drilling in 62 holes less than 48 meters deep from La Lechoza, drilled in the 1980’s. However, while the assays were recovered, the collar locations remain uncertain. In 2002, MIM estimated the collar locations based on the location of the old drilling roads. While the data has provided useful points for exploration, it is not considered reliable (pers. comm., H. Dominguez, Manager for Everton Minera Dominicana), and has been excluded from this report.

Between 15 October and 15 December, 2006, Everton Minera Dominica completed an airtrack reconnaissance drilling program on the Jobo Claro concession. A total of 96 short holes with an average depth of 14 meters, and a maximum depth of 32 meters were completed. The depth of penetration was mainly determined by the position of the water table. Overall, 1404 meters were drilled, and 664 samples were sent for analysis. Collar locations are shown in Fig 11.1. Results from the airtrack drilling at Jobo Claro were negative.



11.2 Diamond Drilling

The Property was first drilled by Pan Ocean Minerals in 1979. Logs of the diamond drill holes are on file at the offices of CMD but no analytical results are available. The locations have been found by Everton, and these are plotted as purple squares on Fig. 11.1. Nelson (2004) reviewed the logs and reports “…drill logs record the presence of disseminated pyrite and massive sulfide (as veins or beds up to 30 centimeters in thickness). Host rocks include silicified and propylitized (chlorite plus epidote), locally amygdaloidal, mafic volcanic flows. The sulfide assemblage (locally as much as 30% by volume) includes pyrite, chalcopyrite, and sphalerite”.

In 1999, CMD completed 659.6 meters of diamond drilling in four holes on the Los Hojanchos concessions (holes LH1‐4). No information is available regarding the machine used or the procedures followed. The original logs were not made available to the author of this Report, but Nelson reviewed both these and the core for Everton in 2003. Nelson (2004) reports “All of the CMD drill holes intersected sulfide mineralization including disseminated fine grained pyrite, local massive sulfide fragments, and cross cutting pyritic veinlets. Recoveries were not recorded but a review of the core indicates that recovery in each of the holes averaged over 95%. The best known overall intercept was 1.6% Cu across 1.2 m in hole LH‐01. Intercepts from LH‐03 might be substantially better, but the copper values exceeded detection and were not re‐measured (Table 9.3).

In December of 2002, MIM contracted Major Drilling Company to drill five core holes that winter and an additional four holes during April‐May of 2003. No mention is made of what machine was used. The holes ranged in depth from 122 to 235.6 meters deep. A total of 1634.4 meters of drilling was completed in roughly 56 days using two 12 hour shifts per day (holes LL‐01 to LL‐08 and C‐01). The calculated production rate was 29 meters per 24 hour day. Drilling was slowed by the blocky and fractured nature of the ground. Where possible, the holes were started with HQ systems and then reduced to NQ, however the broken ground required that some holes be completed entirely with HQ (Rowe, 2003). The author of this report does not have access to the original logs, and does not know what the core recovery was, but no problems were specifically mentioned in MIM’s Report (Rowe, 2002). In a memo dated 29 February, 2002, however, Philip Pyle, V.P. Exploration for Linear Gold mentions:

“Hole LL‐03a is an incomplete thickness of the gold mineralized zone, as it was recovered below a 6.6 meter section with no core recovery due to driller error. Hole LL‐o3b was begun 1.5 meters from the collar of LL‐03a and therefore represents a more complete representation of the same section.

Hole LL‐04 had no core recovery between 11.58‐13.41 (1.83 meters) which is located in the gold bearing zone. This may have added or subtracted from the actual grade of the zone (quoted as 10m @1.02gAu/t).”

Results of the 2002‐2003 drilling are in Table 9.4, One of the best intercepts of this campaign was 1.3 g/t Au, 8 g/t Ag and 0.2% Cu across 30 m in Hole LL‐03b (from 8 to 38 m). There is still some uncertainty about the overall orientation of the mineralization at La Lechoza, and the true width might be smaller than 30 meters.

In September of 2004, Linear Gold contracted Kluane International Drilling (Kluane) to drill 6 holes (APV04‐01, 03, 05, 08, 10 and 12). Kluane provided two portable all‐hydraulic drilling units capable of drilling NTW diameter core to 250 meters and BTW to 350 meters depth. The holes ranged from 193.6 to 341.4 meters deep. A total of 1540 meters of drilling was completed in roughly 42 days using two 12 hour shifts per day. The average production rate was 18 m per 24 hour day per rig. Drilling was slowed by hard silicified zones encountered in the holes. The light‐weight drill did not have sufficient weight to easily punch through these zones (Druecker and Rowe, 2005). The only potentially economic result of this campaign was 0.9% Cu across 10 m in APV04‐12 from 42 to 52 meters (Table 9.5 and Fig. 9.5). Electronic core logs are preserved in the report of Druecker and Rowe, 2005, and the author has reviewed the core from APV04‐08 (Appendix 2).

In September of 2004, Everton and CMD contracted Kluane to drill five diamond drill holes on the Los Hojanchos concessions. The holes were designed to test an IP anomaly underlying weakly anomalous gold geochemistry in soil (Espaillat, J., 2004). A total of 585.57 meters of drilling were completed with weak results (Table 9.3). The geologist in charge recommended drilling for massive sulfides near the old Pan‐Ocean holes (Fig. 11.1).

In April of 2005, Linear Gold Caribe S.A. drilled 3 holes into Mermejal‐La Cueva using one of Kluane’s man‐portable drill rigs. A total of 439.43 meters were completed with negative results. The electronic logs are available, but there are no reports, maps or interpretations.

Between June and November of 2005, Linear Gold Caribe S.A. completed 1858 meters of drilling in 18 diamond drill holes at La Lechoza (LE holes). The author has reviewed the electronic logs, but has not seen the drill core from this campaign.



Linear Gold did not write a Report detailing the drilling procedure, machine used, rates or core recovery achieved or any interpretation of the results. The author has compiled the assays, and these are in Table 9.4. Overall, the campaign was very successful with 14 potentially payable intercepts in 18 holes. One of the best results was 1.5% Cu, 2% Zn, 0.5 g/t Au and 8 g/t Ag across a true width of 14.2 m (Fig. 9.5). They also drilled an additional 276.44 meters in 3 holes at the Tres Bocas prospect (TBM‐01 to TBM‐03). The work was completed in 5 days with production rates of 55.3 meters per day (Dominguez, 2008b). Core handling procedures are documented in Amireault (2006), and these procedures apply to the rest of the holes drilled on the Property after 2005. Two of three holes intercepted potentially economic mineralization. The best result was 1.7 g/t Au across 6 m in Hole TBM‐03 (Table 9.1).

Between 2006 and 2008, Everton Minera Dominicana completed an additional 3098.6 meters of drilling in 35 more holes at Loma El Mate (TBM and TB holes). All except the two 2008 holes were drilled by Kluane International Drilling. In 2008, Sococo, a subsidiary of Major Drilling, drilled holes TBM 27 and 28. The best overall intercept was 1.7 g/t Au, 62 g/t Ag, 1.2% Cu and 6.9% Zn across 19.42 m in Hole TBM‐07 (Table 9.1).

In late 2007, Everton and CMD hired Kluane to drill gold‐rich sulfide targets on the Cuance concession. Overall, 1003.6 meters of drilling in 8 holes were completed by early 2008 (Carrasco, 2008). Payable intercepts are polymetallic with significant precious metals, and are listed in Table 9.2. The best overall intercept was 1.1 g/t Au, 3 g/t Ag, 0.3% Cu and 2.0% Zn across 18.00 m in Hole CUA‐04 (Fig. 9.2).

After drilling Cuance, the focus of Everton’s exploration efforts shifted to the APV concession, probably to comply with the terms of the 2007 earn‐in deal with Linear Gold. Between 2007 and 2010, an additional 3866.76 meters of drilling in 39 holes had been completed, mainly in La Lechoza by Sococo Drilling. To date, there are 42 potentially economic polymetallic intercepts with significant precious metals at La Lechoza (Table 9.4). The best overall intercept was APV 09‐24 with 583 g/t Ag, 0.4 g/t Au and 0.2% Cu across 17 m.

Photo 11.1. AIRTRACK DRILL. This machine was capable of drilling to the water table (maximum depth = 32 meters) vertical holes.

Photo 11.2. MAN PORTABLE DRILL RIG drilling APV 07‐01 (central APV sector). Kluane’s machines can drill BTW core to a depth of 350 m.



Fig. 11.1 Drill collar location plan. The JC holes are Jobo Claro airtrack drill holes, the purple squares are Pan‐Ocean diamond core holes, and all other holes are diamond drill holes drilled by Everton and its partners.

12.0 Sampling Method and Approach

12.1 Soil Samples

On the Property, B‐horizon residual soil samples were collected on pre‐determined survey grids. Sample density and spacing are described in Section 10.2. The samplers navigated using Garmin e‐Trex GPS units and a Silva sighting compass and the pre‐determined GPS waypoints were plotted on a topographic base map for survey control. Each sample site was marked with a painted survey stake, a metal tag with the sample number and pink flagging tape.

Samples were collected by cleaning the organics off the sample site, then digging a small pit about 70 cm deep into the B horizon with an open auger. The samplers were trained how to identify the B horizon, and instructed not wear any metal jewelry to avoid sample contamination. About 1 kg of material was collected from the bottom of the sample pit and put in a sample bag with a numbered tag. At the end of the day, the samplers logged their sample locations on the computer and packaged the samples for transport to the laboratory.

The author has walked over parts of the grid, and verified that the Everton samples are located correctly, and that appropriate material was sampled. It is that author’s opinion that the soil sample database is of good quality and reliable.



12.2 Rock Samples

About 6000 Ha of the Property has been prospected by Everton and its partners with rock geochemistry. On the APV concession, most bedrock exposures have been sampled to evaluate lithological variations and variations in alteration mineralogy using a PIMA spectrometer. On the other concessions, rock samples are mainly from mineralized outcrops. Several types of rock samples were used in the evaluation of the Property, and these are listed in Table 12.1. For all types of samples, 1 to 2 kilograms of rock chips were collected in a durable plastic sample bag with a numbered tag. Samplers were instructed not to wear metal jewelry to avoid sample contamination.

Hand dug trenches at Los Hojanchos and Cuance measured 2 meters deep and one meter wide. Continuous samples were collected at two‐meter intervals from a 6 centimeter channel cut into the bottom of the trench. Mechanically dug trenches at La Lechoza were as deep as 3 to 4 meters, but the sampling procedure is the same.

Geochemical data from surface rock samples is very difficult to duplicate, mainly due to the natural variability of geological materials. Causes of variability include: (i) irregular distribution of quartz veining or sulphides, (ii) variable effects of surface weathering, (iii) sample face preparation – removal of organics and oxides, (iv) the ability of the geologist to locate a representative sample, (v) the tools the sampler is using, and (vi) the strength and ability of the sampler to provide a regular cut of the sample. Because it is pretty much impossible to duplicate surface rock geochemistry, the results are treated as semi‐quantitative. Having said that, maps of both the rock samples and the soil samples show the same anomalies , so the data are considered to reliable and of good quality.

Table 12.1 Types of rock samples used to evaluate mineral occurrences on the Property.

SAMPLE TYPE DESCRIPTION AND COLLECTION METHOD

Grab Samples A sample taken from an outcrop, but not oriented across a structure, and not necessarily representative.

Float Samples A rock sample from loose material, usually stream boulders or colluvium.

Chip Samples Oriented samples taken across a width by chipping pieces of rock approximately every 10 cm.

Chip‐Channel Samples Oriented samples cut across a representative part of a mineralized structure using a sledgehammer and chisel to form a continuous channel. These types of samples are also used in trench samples.

12.3 Percussion Drill Samples

Samples from the airtrack drill were circulated to surface using compressed air, and samples were captured every 2 meters. The sample weight varied from 1 to 5 kg. The material was split to about 1 kg using a splitter box, and the 1 kg split was packaged for transport to the lab, with the remaining material kept on‐site. Finally, visual reference samples were prepared by placing a spoonful of chips in labelled RC chip trays.

Air track drills are designed for drilling 30 meter long blast holes for quarrying operations, and are not designed for quantitative geological sample collection. Nonetheless, the method is very fast, and provides qualitative, near‐surface information that can be used to design diamond drill programs for quantitative mineral resource and reserve estimation. The information is qualitative for the following reasons:

A set sample length is used, so the boundaries of the mineralization are not known precisely.

The cuttings are lifted to surface using air. When coarse gold is present, the circulation of the fluid will cause it to settle to the bottom of the drill hole. Therefore, the gold assays of the cuttings can under‐report the amount of gold actually present.

Material from the upper parts of the hole can fall into the hole and contaminate the sample.

12.4 Diamond Drill Samples

The following core handling and sampling method was observed by Everton. As core was received from the contractor, it was examined and logged by a geologist at either the drill site or the exploration facilities at Cotuí. The sampling interval was marked with tags and a small piece of PVC pipe on which was written the sample number, from‐to footage, and the date, all in waterproof ink. The following tools were used to split the core: (i) electrical diamond saw, (ii) hydraulic splitter, (ii) blade, (iii) hammer, and (iv) chisel. The selection of which tool to use depended mainly on the condition of the core,



with hard core responding best to the diamond saw or hydraulic splitter, and soft mushy cores being better split with hand tools.

For drill holes from Cuance and Los Hojanchos, core was sent to CMD’s Falcondo facilities where it was cut by an electrical core saw. Half the core was placed in a plastic bag that was numbered, tagged and sealed. Geologists could request the return of the boxes at any time for additional detailed logging. The numbered samples were sent to Chemex for analysis. Starting in 2008, Everton switched the assaying from the Globestar Properties to ACME.

Sample widths ranged from 1 to 2 meters, with some adjustments to accommodate geological and mineralization boundaries.

Recovery of the core was generally better than 90%, except in laterized zones at the top of the hole where recovery can be poor due to the weak and fractured nature of the rock. In most holes, the laterites are less than 20 meters thick. In La Lechoza, where part of the potential gold resource is in oxides, poor recovery at the top of the hole can affect resource estimates.

13.0 Sample Preparation, Analysis and Security

13.1 Soil samples

Soil samples collected by Everton were sent to Acme’s sample preparation facility in Maimón where they were oven‐dried at 60°C, then sieved to produce 100 grams of pulp at less than –80 mesh. The prepared pulps were then shipped via DHL to the Vancouver lab for analysis. In Vancouver, a 15 gram sample was dissolved in hot aqua regia and analysed using ACME’s 1F ICP‐MS package for gold and base metals (Dominguez, 2008a).

Soil samples collected by CMD from Los Hojanchos and Cuance were dried, crushed and pulverized to minus 100 mesh at the Falcondo laboratory in the Dominican Republic. The pulverized sample was then shipped to Chemex Laboratory in Toronto for a 32‐element ICP package plus gold analysis using a fire assay fusion followed by atomic absorption analysis (Nelson, 2004).

13.2 Percussion drill samples

Percussion drill samples for analysis were shipped via air freight to Laboratoire Experts en Rouyn Noranda, Quebec, Canada for gold fire assay. ICP multi‐element analysis was completed by Activation Laboratories in Mississauga, Ontario, Canada (Dominguez, 2007).

13.3 Rock and core samples:

Once Everton’s samples are delivered to ACME’s Maimón facility, all sample preparation is handled exclusively by ACME. All rocks and core samples are prepared by crushing to 70% passing 10 mesh, then a 250 g split is prepared and that is pulverized to 85% passing 200 mesh. The prepared pulps were then shipped via DHL to the Vancouver lab for analysis. In Vancouver, a 15 gram sample was dissolved in hot aqua regia and analysed using ACME’s 1DX ICP‐MS package for gold and base metals (Dominguez, 2008a). Oversize rejects are kept in storage at Acme laboratories Maimón facilities.

Rock and core from the Cuance and Los Hojanchos concessions were taken to the Falcondo facilities in Bonao where the core was crushed, pulverized and sieved to minus 200 mesh. Duplicate pulps, 300 g each, were routinely prepared and returned along with coarse rejects to Maimón to be stored at the Globestar core shack. The pulps were sent by DHL to an ALS Chemex laboratory. In 2005, assays were done in Mississauga, and in 2006 they were sent to Vancouver. Gold was analyzed by 30‐g fire assay (method AA23 of ALS Chemex). Base metals were assayed using Induced Coupled Plasma (ICP41 of ALS Chemex). Half‐core samples from Loma El Mate were bulk air‐freighted to ALS Chemex in Vancouver where they were crushed, and a subset of the sample was pulverized to minus 200 mesh. The pulp was assayed for gold (30‐g fire assay, method AA23 of ALS Chemex) and for base metals (Induced Coupled Plasma, method ICP41 of ALS Chemex). In all cases, a tight security was maintained for the handling of the core. One of the company representatives picked up the boxes on‐site and transported them to either Maimón or Cotuí where the core boxes are now stored. Both places are secured and manned.



Minera Camargo collected a single batch of 39 rock samples and 6 ¼ core samples, and inserted two WCM Pb125 control standards into the batch. The rocks were then shipped to Acme Laboratories’ preparation lab in Guadalajara via Multipack couriers from Mazatlán, Sinaloa, Mexico. Acme has a quality system compliant with the International Standards Organization (ISO) 9001 Model for Quality Assurance and ISO/IEC 17025 General Requirements for the Competence of Testing and Calibration Laboratories. At the lab, the samples were dried, crushed, split and pulverized and a thirty gram charge prepared from the pulp. The prepared pulps were shipped to Vancouver via DHL, and analyzed using the 1DX ICP‐MS package at Acme's Vancouver lab. Gold values greater than 500 ppb were fire‐assayed for Au (Group 6), and base metals greater than 10 000 ppm were re‐analyzed using ICP‐ES (Group 7) methods. Analytical certificates are in Appendix 3.

14.0 Data Verification Everton inserts blank limestone samples into the sample stream. No standards or duplicate samples are used. Camargo checked the blank results for diamond drill holes APV09‐22, APV10‐02 and APV10‐06 (Table 14.1). The limestone has low, but non‐zero metal concentrations which are estimated by the average value. Values higher than the mean plus 2 standard deviations (UPPER LIMIT) from the mean might reflect either (i) sample contamination has occurred in the lab, or (ii) that one of the limestone samples has some mineralization in it. In the sample set of Table 14.1, the highest gold value is 6.9 ppb, which is 1.5 ppb higher than the upper limit. Similarly there is one sample with a value of 21.3 ppm Cu, and one with 42 ppm Zn. As all of these are different samples, and the absolute amount above the upper limit are small, there appears to be no systemic contamination. The author of this report asked Everton’s manager if he had ever had to repeat a batch due to contamination issues, and the answer to that question was negative (pers. comm. H. Dominguez, 2010).

Table 14. 1 Limestone Blank Sample Data. Hole_ID Certificate Sample Number Ag_ppm Au_ppb Cu_ppm Zn_ppm

Detection Limit for the 1DX ICP‐MS method

0.3 ppm 0.5 ppb 0.1 ppm 1 ppm

APV10‐02 DRG10000032 311065 0.1 0.5 2.1 3

APV10‐02 DRG10000032 311080 0.1 1.3 21.3 3

APV10‐02 DRG10000032 311095 0.1 0.7 10.2 14

APV10‐02 DRG10000032 311210 0.1 0.5 4.2 5

APV10‐02 DRG10000032 311225 0.1 0.7 1.6 13

APV10‐06 DRG10000064 311430 0.1 1 14.4 42

APV10‐06 DRG10000064 311445 0.1 1.7 4.7 10

APV10‐06 DRG10000064 311460 0.1 6.9 1.9 6

APV10‐06 DRG10000064 311475 0.1 0.5 2.9 6

APV‐09‐22 DRG000572 310410 0.1 3.7 2 4

APV‐09‐22 DRG000572 310425 0.1 0.5 8.9 3

AVG 0.1 1.6 6.7 10

STDV 0 1.9 6.1 11

2STDV 0 3.8 12.2 22

AVG+2StdDev (UPPER LIMIT) 0.1 5.4 18.9 32

To estimate the general sampling error of the diamond drill core, Minera Camargo took a ¼ core split of six samples. The results are in Table 14.1. All of Camargo’s samples contained less gold than Everton’s, but copper, zinc and silver values don’t show any systemic bias. Overall, the results are in the range expected given that the mineralization is not homogeneous and that there may have been some shifting around of the core while it was in storage. It is Minera Camargo’s opinion that the data are reliable for Ag, Cu and Zn, but that there is a small amount of uncertainty about the reliability of the gold analyses that could be removed by including gold standard materials in the sample stream.



Table 14. 2 Repeat ¼ core samples. HoleID From (m) To (m) Sample Number Ag (ppm) Au (ppb) Cu (ppm) Zn (ppm)

TBM‐07 20.2 21.8 19652 160 7750 17400 134000

19652R 60.9 2684 19050 199500

REL. DIFF 90% 97% 9% 39%

APV10‐02 24 25 311073 3.7 267.3 20980 241

311073R 4 205.9 16210 262

REL. DIFF 8% 26% 26% 8%

APV10‐02 104.5 105.5 311239 0.4 40.2 37 458

311239R 0.4 24.1 81.6 419

REL. DIFF 0% 50% 75% 9%

APV10‐06 13.5 14.25 311426 11 982.3 13130 9200

311426R 8.2 657.7 13000 9250

REL. DIFF 29% 40% 1% 1%

APV10‐07 9.5 11 311502 410 866.8 2110.2 329

311502R 486 818.2 2174.2 266

REL. DIFF 17% 6% 3% 21%

APV10‐07 14 15 311506 22.4 357.3 35310 8030

311506R 20.6 292 28520 9247

REL. DIFF 8% 20% 21% 14%

Finally, Camargo analysed 113 small core specimens for base metals with the Niton GOLDD hand‐held XRF (Appendix 2). While these results cannot be compared directly to quartered and homogenized samples, they do confirm the overall tenor of the mineralization, and order‐of‐magnitude estimates for copper and zinc concentrations from the Niton are very similar to the assay results. Therefore, Camargo believes that the

Amireault (2006) re‐ran rejects from high grade intercepts in TBM‐07 and TMB‐12. The reject results showed good repeatability of metal concentrations and he concluded that the data were of good quality.

CMD routinely inserted blanks and standards in the sample stream. Results were reviewed by Nelson (2004), and he concluded that their data was reliable.

15.0 Adjacent Properties

15.1 Pueblo Viejo

The APV concessions surround the Pueblo Viejo gold deposit. Historically, the Pueblo Viejo deposit has produced over 5 million ounces gold, largely from oxide ore. The latest published reserve estimate for the Monte Negro and Moore Pit (combined) is 248.6 million tonnes of ore grading 2.8 g/t Au, 13.4 g/t Ag, 0.56% Zn and 0.08% Cu. (measured and indicated categories at a 1.4 g/t Au cut‐off grade; Smith et al., 2008). The author of this Report has not verified this information and this information is not necessarily indicative of the mineralization on the Everton’s APV Property. Partners Barrick Gold Corporation and Goldcorp Inc. are currently constructing an open‐pit mining complex on the site. Current plans are to have the mine in production by the end of 2011 (Barrick Gold Corporation Annual Report, 2009).

Mineralization and alteration in the Pueblo Viejo protore was formed by a submarine VMS system within the Late Cretaceous Los Ranchos Formation. The protore consists of thinly laminated sulfide (mainly pyrite) in black carbonaceous sediments of marine origin (Photo 15.2) developed in anoxic basins next to argillic‐altered rhyolite flow‐domes (Photo 15.1). A 2 meter thick sample of the massive sulfide contains 4.6 g/t Au, 280 g/t Ag, 0.01% Zn and 0.05% Cu (Kesler et al., 1981). The massive sulfides are cross‐cut by white to pink chalcedonic quartz veins with about 10‐20% pyrite (Photos 15.2 and 15.3). An early test of 12 hand‐picked samples of laminated pyrite from massive sulfide yielded an average result of 8.9 g/t Au and 72 g/t Ag compared to an average result of 72 g/t Au and 230 g/t Ag for a similar number



of samples of pyrite samples from veins (Kesler et al., 1981). The age of the quartz veins was estimated by 40Ar/39Ar isotopic testing of co‐genetic alunite from a quartz‐alunite‐pyrite vein about 205 meters below the present surface. Measurements indicate that the alunite has a Late Cretaceous to Tertiary age between 67.8 +/‐ 0.8 Ma and 61.6 +/‐ 0.9 Ma (Kesler et al., 1981). Diorite and quartz diorite plutons related to Late Cretaceous to Tertiary calc‐alkaline volcanism on Hispaniola range from 80 to 60 Ma, and are coeval with epithermal quartz veining.

Photo 15.1. PUEBLO VIEJO. Argillic altered Zambrana rhyolite dome. Sample 25627, cut from the grey area above the talus, contains 42.8 g/t Ag and 356 ppb Au (Appendix 1). Alteration minerals are dickite and kaolinite. The rhyolite is characterized by silicified “domains” (spherulites) about 3 mm across that are surrounded by arcuate perlitic fractures.

Photo 15.2 PUEBLO VIEJO. Photo of laminated massive sulphide protore cross‐cut by white quartz veinlets (photo from Hedenquist and White, 2005). Gold grades at Pueblo Viejo are closely associated to the late veins (Kesler et al., 1981).

Photo 15.3 PUEBLO VIEJO. Fairly flat lying carbonaceous quartz‐crystal tuff. The wall rocks to the vein are pervasively altered to dickite, and cross‐cut by a vein of white to pink quartz with finely crystalline, dirty pyrite oriented 138˚/90˚. A random sample of the argillite contains 1531 ppm Zn and 246 ppb Au (sample 25618; Appendix 1). A sample across the 0.3 m wide vein in the photo contains 2.8 g/t Au, 5.2 g/t Ag and 1319 ppm Zn (sample 25621; Appendix 1).

Photo 15.4 PUEBLO VIEJO. View of sub‐vertical diorite dike of probable Tertiary age in the Monte Negro pit. The dike has aphanitic chilled margins, and the core contains about 30% zoned feldspar phenocrysts 5 to 10 mm long. The rock is altered to kaolinite and illite (argillic assemblage), and contains 1% disseminated pyrite. A sample from the center of the dike contains 81 ppb Au (sample 25620). These dikes might be feeders to coeval Late Cretaceous‐Tertiary basalts.

15.2 Cerro de Maimón

Cerro de Maimón is a volcanogenic massive sulfide deposit hosted in the Cretaceous Maimón Formation located about 8 km west of the Cuance concession boundary. The ore consists of two parts, a massive sulfide body and an oxide cap. The massive sulfide body contains 4.8 million tonnes of proven and probable ore grading 2.54% copper, 0.96 grams per tonne gold and 34.9 grams per tonne silver. The oxide body contains 1.2 million tonnes of proven and probable ore grading 1.86 grams per tonne gold and 34.5 g rams per tonne silver. Globestar started mining the deposit in 2008



(http://www.globestarmining.com). The author of this Report has not verified this information and this information is not necessarily indicative of the mineralization on the Everton’s APV Property

16.0 Mineral Processing and Metallurgical Testing No metallurgical testing has been done.

17.0 Mineral Resource Estimates To the author’s knowledge, there is no mineral resource or reserve calculated for the Property. However, several significant drill hole intercepts obtained by Everton and its partners suggest that there is potential to outline a mineral resource(s).

18.0 Other Relevant Data and Information The author of this report is not aware of any additional information, the omission of which would be misleading. While there is believed to be additional geological, geophysical and geochemical information concerning the Properties that may be in the possession of Everton Resources or subsidiaries or partners, in the author’s judgment sufficient information has been supplied for this Technical Report.

19.0 Interpretation and Conclusions The APV Project surrounds the Pueblo Viejo mine in all directions except south. The in‐situ metal value of the Pueblo Viejo deposit is in excess of $30 billion USD at today’s metal prices, and more than 80% of the value is in gold, with the rest of the value in zinc, silver and copper. Under most classification systems, Pueblo Viejo is a giant gold deposit, and about 40% of giant deposits are intrusion‐centered (Hedenquist and White, 2005). The center of the intrusion that might have been related to gold deposition at Pueblo Viejo is thought to occur under a strong anomaly in the Earth’s total magnetic field that is about 3.5 kilometers in diameter and centered on the southern part of Everton’s APV concession. Drill holes in this area do not intercept intrusive rocks, therefore, this hypothetical intrusion is buried deeper than 300 meters. The conclusion that the mineralization is intrusion‐related is strongly supported by the presence of a thick lithocap of advanced argillic (pyrophyllite) altered rocks that caps both the Pueblo Viejo deposit and extends northwestward for another 11 kilometers onto Everton’s concession. Lithocaps of this type occur in the upper parts of porphyry copper systems (Sillitoe 2010; Fig 8.3), and are not known to occur in other geological environments. The formation of pyrophyllite is significant as it usually forms in non‐buffering (felsic) rocks by reacting with a cooling of a sericite/muscovite stable fluid as it cools and migrates upwards from the magmatic source through the overlying and surrounding rock column. SWIR analyses of 10 rocks from the Monte Negro gold mine show that the alteration in the vicinity of the open bit is dominated by sericite (8 of ten samples contain sericite and only two contain pyrophyllite), so it could be that gold deposition is mainly controlled by the thermodynamic boundary that is marked by the transition from sericite/muscovite alteration to pyrophyllite alteration, with minerals such as dickite (deposited from cooler, even more acid fluids) mainly close to open spaces such as veins. The pyrophyllite boundary marks several thermodynamic changes that can de‐stabilize any gold in solution and cause it to precipitate: (i) a drop in temperature, (ii) a drop in pressure and (iii) a pH drop that forms the acid solutions responsible for the advanced argillic alteration up‐section. On Everton’s Property, this thermodynamic boundary occurs about 1700 meters northeast of hole APV04‐05, and can be estimated by using the barium‐in‐soil map. Barium substitutes for potassium in K‐mica (illite or muscovite) and highlights areas that might be affected by potassium metasomatism (sericitization).

Another factor that probably contributed to the unusual size of Pueblo Viejo is deposition of a layer of rocks rich in synsedimentary sulfides and biogenic carbon (Pueblo Viejo Member). Both sulfides and carbon will react with any gold in solution and cause it to precipitate into the rock. Everton has located outcrops of the Pueblo Viejo Member on the eastern boundary of the southern part of the APV concession, in the central part of the APV concession about 500 meters south of APV09‐09 and on the western boundary of the southern part of the APV concession. Due to the soft and recessive nature of these rocks, they are very difficult to find on surface and outcrops are sparse. While the author has drawn the Pueblo Viejo Member on the geological plan (Fig. 7.3), this plan is expected to change as further drilling better defines the location and thickness of this important rock unit which probably acted as a gold trap.



North and west of Pueblo Viejo, several VMS prospects have been identified on the APV project: (i) La Lechoza, (ii) Cuance, (iii) Los Hojanchos and (iv) Tres Bocas. Of these, La Lechoza is the best defined, and there is near‐term potential to develop a polymetallic resource there with additional drilling down dip of the known intercepts. However, the most compelling VMS story is the zoned but untested geochemical anomaly in the area of historic Pan‐Ocean drill holes at Los Hojanchos. In this area, anomalous zinc and copper geochemistry defines an area about 2 kilometers long and 1.3 kilometers wide, with copper‐rich geochemistry occurring to the northeast (in the footwall), and zinc‐rich geochemistry below a basalt flow in the hanging wall (Figs. 9.3 and 10.3). The bottoms of volcanic flows in the tuffaceous rocks of the Maimón formation are thought to be especially prospective as these can cap hydrothermal solutions which then pond below the impermeable volcanic flow, cool and deposit metals (e.g. Gifkins, 2005). This geologic situation occurs at both Cuance and Loma El Mate (Figs 9.2 and 9.1).

20.0 Recommendations Everton Minera Dominicana’s core business plan for 2010‐2012 is twofold: (i) drill through the lithocap and explore for on‐strike and down‐dip extensions to Pueblo Viejo as that could be where the highest potential value of the Project is located, and (ii) explore and expand the known VMS mineralization elsewhere on the Property, mainly by drilling. The Budget allows for the use of a D‐6 tractor to build access roads and drill pads, although it may be easier from a permitting perspective to use a man portable drill in some locations. Overall, two phases of exploration drilling are planned. The first phase consists of 11 280 meters of drilling in 76 holes, with a maximum hole depth of 450 meters. Overall Phase 1 costs are estimated to be $4.0 million USD (Table 20.1). The second phase of drilling consists of 18 035 meters of drilling in 43 holes, with a maximum hole depth of 900 meters. The decision to attempt the deeper holes through the lithocap depends on the results of the first phase of drilling, particularly the interpretation of rock alteration vectors. Alternatively, the Phase 1 results might justify upgrading one of the prospects to an NI 43‐101 compliant mineral resource estimate. Overall, Phase 2 costs are estimated to be about $6.0 million USD (Table 20.2).

Other general recommendations are:

Purchase of one or two portable Niton XRF units that can reliably measure base metal concentrations (but not gold) is recommended for in‐field prospecting and dynamic drill hole control. The instrument can pay for itself by eliminating most unnecessary assays and database maintenance costs, as well as eliminating the wait time between sample collection and (base‐metal) analysis. Only about 10% of the core is payable mineralization, and Everton is currently assaying more than 80% of the core. This could probably be reduced to 30% without jeopardizing the integrity of the Project.

Installation of a binocular microscope with camera attachment in the core facility. Combined with the PIMA spectrometer and XRF, the equipment will eliminate most errors in mineral and rock identification. The gear will require air conditioning, so the core‐processing facility has to be improved or moved, and a reliable 24 hour power source installed. This in‐house lab should be used to analyze all rocks from surface mapping programs as well as all drill core.

Inclusion of gold‐standard materials in the sample stream.

Improve quality of gold assays by changing the assay method of mineralized core from semi‐quantitative 1DX to quantitative fire assay (Groups 3 [low grade] or 6 [higher grades]).

Where oxides might be part of a resource estimate (La Lechoza), holes could be collared with “P” size core for 20‐30 meters. This will probably minimize recovery problems.

Further surface geophysical surveys are not especially recommended to target drill holes, although down‐hole EM or IP surveys might prove useful. Geochemistry and alteration analysis (using the PIMA) are expected to be more effective, both in the lithocap and on the VMS prospects particularly as these vectors become defined in the core. In the VMS environment, any identification of phengite or andalusite with anomalous zinc or copper is enough to define a potential drill target.

Concurrent with the drilling, there should be a sustained geological mapping and sampling effort made (or at least supervised) by senior geologists complemented by any in‐house and external lab analyses required to “get the map right”. In particular, resolving the age and origin of different mafic rocks on the Property is critical as Late‐Cretaceous‐Tertiary diorites and basalts are probably related to gold mineralization. Previous mappers (Kesler et al, 1981) have mapped basalts in the vicinity of Pueblo Viejo as Cretaceous Los Ranchos Formation, but the author of this report thinks they may be co‐genetic with the later mafic dikes that cross‐cut the open pits.



Table 20.1 Summary of proposed Phase 1 Drilling Expenditures for the APV Project.

ITEM COST IN USD

Environmental Permitting, Land Access $ 24,956.23

2 Niton XRF assayers $ 100,000.00

Binocular microscope with Camera $ 10,000.00

Access and drill pad construction (both Phases) $ 152,807.78

Geological Mapping $ 536,000.00

Diamond Drilling (11,280 m) $ 2,495,623.33

Petrography/Metallurgy $ 24,956.23

Reporting (Geological Modeling) $ 49,912.47

Subtotal $ 3,394,256.04

Management/Admin (15%) $ 509,138.41

CSR/Reclamation (3%) $ 101,827.68

TOTAL $ 4,005,222.13

Table 20.2 Summary of proposed Phase 2 Drilling Expenditures for the APV Project.

ITEM COST IN USD

Environmental Permitting, Land Access $ 43,674.47

Diamond Drilling (18,035 m) $ 4,367,447.22

Down‐hole geophysics $ 500,000.00

Petrography/Metallurgy $ 43,674.47

Reporting (Geological Modeling, possible Resource Estimates)

$ 131,023.42

Subtotal $ 5,085,819.58

Management/Admin (15%) $ 762,872.94

CSR/Reclamation (3%) $ 152,574.59

TOTAL $ 6,001,267.11



Fig. 20.1 Exploration diamond drilling plan overlaid on a geochemical anomaly map. YELLOW=Au in soil >28 ppb, BROWN=Zn in soil > 230 ppm, CYAN=Cu in soil >130 ppm, GREY=Mo in rock and soil >25 ppm. Red dots are payable diamond drill intercepts. Red outlines are open pit gold mines.



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Dubé, Benoit, Gosselin, P., Mercier‐Langevin, P., Hannington, M., Galley, A., 2007, Gold‐rich volcanogenic massive sulfide deposits; in Mineral Resources of Canada: A synthesis of major deposit‐types, district metallogeny, the evolution of geological provinces, and exploration methods; Geological Survey of Canada, Mineral Deposits Division of the Geological Association of Canada, Special Publication No. 5, p.75‐94.

Espaillat, J., 2004, Summary report on the 2004 exploration and drilling programs on the Los Hojanchos concession; Corporación Minera Dominicana, S.A.; internal Company report, 15 p.

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Gifkins, C., Herrmann, W., Large, R., 2005, Altered Volcanic Rocks; a guide to description and interpretation: Center for Ore Deposits Research, University of Tasmania, Australia, 275 pages.

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Hedenquist, J.W., White, N.C., 2005, Epithermal gold‐silver deposits: characteristics, interpretation, and exploration; Prospectors and Developers of Canada and Society of Economic Geologists Short Course Notes.



Herrmann, W., Blake, M., Doyle, M., Huston, D., Kamprad, J., Merry, N., Pontual, S., 2001, Short wavelength infrared (SWIR) spectral analysis of hydrothermal alteration zones associated with base metal deposits at Rosebery and western Tharsis, Tasmania, and Highway‐Reward, Queensland; Economic Geology, v. 96, p. 939‐955.

Holbek, P.M. and Daubeny P.H., 2000, Geology of the San Antonio Concession, Dominican Republic in Sherlock, R.I. and Logan, M.A.V., (eds.), VMS Deposits of Latin America; Geological Association of Canada, Mineral Deposits Division, p. 197‐212

Jones, S., Herrmann, W., Gemmell, B., 2005, Short wavelength spectral characteristics of the HW Horizon: Implications for exploration in the Myra Falls volcanic‐hosted massive sulphide camp, Vancouver Island, British Columbia, Canada; Economic Geology, v. 100, p. 273‐294.

Kesler, S.E., Campbell, I.H., Allen, C. M., 2005, Age of the Los Ranchos Formation, Dominican Republic: Timing and tectonic setting of primitive island arc volcanism in the Caribbean region; Geological Society of America Bulletin, v. 117 p. 987‐995.

Kesler, S.E., Russell N., Seaward, M., Rivera, J., McCurdy, K., Cumming, G.L., and Sutter, J.F., 1981, Geology and geochemistry of sulfide mineralization underlying the Pueblo Viejo gold‐silver oxide deposit, Dominican Republic; Econ. Geol. vol. 76, p. 1096‐1117.

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Certificate of Author

I Michelle Robinson do hereby certify that:

1. I am currently retained as an Independent Consulting Geologist by: EVERTON RESOURCES #103‐5420

Canotek Road, Ottawa, Ontario, Canada K1J 1E9 2. My permanent work address is in Mexico. 3. I graduated from the University of British Columbia in 1992 with a BASc. in Applied Science, and in 1994

with an MASc. in Applied Science. I have practiced continuously in my profession for 17 years since 1994 on a variety of deposit types and early to advanced stage exploration projects as well as producing mines.

4. I am a practicing Member of the Association of Professional Engineers and Geoscientists of British Columbia (Lic. #23559)

5. I am a Fellow of the Society of Economic Geologists, a member of the Canadian Institute of Mining and Metallurgy, a core member of the Prospectors and Developers Association, and a member of the Geological Association of America.

6. I have read the definition of “qualified person” set out in National Instrument 43‐101 and certify that by reason of my education, work experience and affiliation with a professional association, I fulfill the requirements to be a “qualified person”.

7. The date and duration of my most recent and first visit to the Property was five full work days between 19 April 2010 to 25 April 2010.

8. As of the date of this certificate, to the best of my knowledge, information and belief, the Technical Report contains all scientific and technical information that is required to be disclosed to make the Technical Report not misleading.

9. I am independent of the issuer applying all of the tests in Section 1.4 of NI 43‐101. I do not have, nor do I expect to receive, directly or indirectly, any interest in the subject property of the Technical Report or any other property discussed in the Technical Report, or securities of Everton Resources, or any affiliated companies.

10. I have read National Instrument 43‐101 and Form 43‐101‐F1, and the Technical Report has been prepared in compliance with that Instrument and Form. The Technical Report has been prepared in conformity with generally accepted Canadian mining industry practice.

11. I am responsible for the preparation of all sections of the report titled “INDEPENDENT TECHNICAL REPORT FOR THE AMPLIACION PUEBLO VIEJO (APV) PROJECT, DOMINICAN REPUBLIC, Latitude 18º54', Longitude 70º06' ” and dated 23 August, 2010.



Appendix 1: Abbreviated listing of surface rock data SAM EAST NORTH ELEV COMMENT LITH MAG ALT. ASSEM. ALT. MIN. Cu_ppm Zn_ppm Ag_ppm Au_ppb

25612 377686 2101233 155 Botryoidal Fe‐oxide, silica. Red to green. Surface weathering product of sulfide.

0.73 Hematite 3174 147 1.9 519

25613 377596 2101143 163 10% feldspar glomerocrysts 3‐7 mm across. 1‐2% round quartz phenocrysts 0.5‐3 mm across, tiny mafics in a finely crystalline (granitic) matrix. Tiny spherulites 2 mm across. Greasy with clay alteration.

10C 0.34 Sub‐Propylitic Montmorillonite 34.5 77 0.1 0.5

25614 377591 2101163 163 Finely crystalline basalt with amygdules and tiny feldspar phenocrysts. Matrix light green with propylitic alteration.

12A 0.91 Sub‐Propylitic Chlorite 4543.5 3913 2.3 12

25615 377576 2101163 164 Hematitic fault zone in Los Ranchos Basalt (Prev. sample of 0.3 m wide had more than 5 g/t Au).

12A 0.15 Sub‐Propylitic Hematite 3040.3 679 9.9 2455

25616 377624 2101146 151 Quartz vein‐breccia. Gemmy quartz with sulfide ‐‐ mainly boxwork filled with limonite, but some chalcopyrite preserved.

V 0.07 Argillic Scorodite 523.3 179 94.2 2095

25617 377924 2101358 154 Rock fragments of cherty silica as well as clay altered rock fragments in a hematitic, earthy matrix.

Bhy ‐0.44 Argillic Kaolinite‐smectite 456.6 256 12.4 932

25618 375180 2095903 364 Thinly bedded, black argillite interlayered with quartz‐phyric crystal tuff and thinly bedded pyrite. Cross‐cut by veinlets of very soft white dickite.

10CFX/1A 0.27 Advanced Argillic Dickite 26.3 1531 0.4 245.8

25620 375061 2095963 373 Andesite porphyry dike. Zoned feldspars, altered to kaolinite. Matrix to moderately crystalline illite. Disseminated pyrite. Cross‐cuts black argillite, chilled margins.

33 0.6 Argillic Kaolinite 65.8 166 0.1 81.1

25621 375070 2095964 376 White to pink chalcedonic quartz vein in black argillite/tuff. Cross cut by clear quartz with finely crystalline, dirty pyrite.

V ‐0.05 Quartz 28.1 1319 5.1 2430

25622 372143 2096977 518 Platanar andesite, "Silica Cap". Rock is pervasively altered to medium crystalline, white pyrophyllite.

50W ‐0.01 Advanced Argillic Pyrophyllite 2 4 0.1 2.7

25623 372442 2096965 538 Platanar andesite, cross‐cut by white, cockscomb quartz with specularite.

11A 2.76 Argillic Illite‐smectite 35.3 2 0.1 5.3

25624 372611 2097108 559 Platanar andesite. Rock is pervasively silicified with specularite veinlets.

11A 0.38 Goethite 18.1 1 0.1 1

25625 372766 2097158 569 Platanar andesite. Rock is pervasively silicified, brecciated with jasper in the matrix.

11A 0.38 Goethite 9.5 2 0.2 2.2

25626 372954 2097181 575 Platanar andesite. Rock is pervasively silicified.

11A 1.19 Goethite 13.3 4 0.1 11.6

25627 376152 2094419 303 Rhyolite with silicified domains, perlitic fractures. Area around domains are altered to white clay.

10C 0.6 Advanced Argillic Kaolinite 59.1 114 42.8 356

25628 376616 2092861 221 Hatillo Limestone. Grey, re‐crystallized, a bit of a clay sheen, but SWIR only sees calcite.

2 0.1 Calcite 1.6 15 0.1 0.5

25629 380094 2088231 173 Rock is schistose quartz with boxwork after sulfide.

50W 0.96 Argillic Quartz 361.4 66 0.6 206.7

25630 386319 2085116 278 Rock is schistose with boxwork after sulfide.

50W 1.6 Argillic Quartz 1246.9 14 1 7.1

25631 385077 2085517 370 Quartz veinlet in sericite schist. Possible lapilli frgs.

10CFX 0.64 Argillic Quartz 47.6 1 1 7

25632 385092 2085510 367 Quartz veinlet in schist. Boxwork due to leaching of sulfide.

50W 0.47 Argillic Quartz 1047 2 2.9 18.4

25633 385176 2085472 359 12% quartz veinlets in schist. Boxwork due to leaching of sulfide.


25634 385219 2085482 359 Quartz veinlets in schist. Boxwork due to leaching of sulfide.


25635 380032 2085614 217 Rhyolite lapilli tuff. Lapilli 3 cm across. Diss. chalcopyrite, foliated.

10CFX 0.35 Sericitic Illite‐smectite 530.5 163 0.7 15.7



25636 380063 2085617 230 Rhyolite lapilli tuff. No quartz phenos. Lapilli 3 cm across. Diss. chalcopyrite, foliated, silicified, shiny illite.

10CFX 0.35 Sericitic Illite‐smectite 398.6 93 1 220.4

25637 380109 2085601 233 Foliated, fine pyritic sediment. ORE HORIZON

50W 0.17 Sericitic Phengite‐smectite 720.1 8114 25.8 3914

25638 380130 2085616 232 Finely crystalline, green rock. Matrix pervasively altered to phengite (Fe, Mg muscovite) and chlorite.

50W 0.05 Sericite‐chlorite Phengite 9.3 207 0.2 0.8

25639 379918 2085724 306 Rhyolite crystal tuff with quartz phenocrysts. Matrix altered to white clay. Site of 2 g/t Au.

10CFX 0.08 Sericitic Montmorillonite 310.6 73 0.7 418.2

25640 379957 2085607 227 Schistose, green rock. Pervasively silicified with chlorite, illite, 3% pyrite stringers

50G 0.38 Chloritic Fe‐chlorite 20.1 81 0.5 21.9

25641 379828 2085407 208 Foliated, white schist with silvery, finely crystalline sulfide.

50W 0.13 Sericite‐chlorite Phengite 860 267 3 183.1

25642 386363 2084358 261 Roughly flat area of gossanous rock.

Argillic Kaolinite‐smectite 876.4 967 0.2 1.6

25643 405255 2087402 147 Basaltic agglomerate. Pervasively silicified, bleached (leached?).

12F 0.15 Argillic Illite 12.8 4 0.1 2.1

25644 405106 2087502 161 Rhyolite with silicified domains, perlitic fractures. Area around domains are altered to white clay.

10C 0.7 Argillic Illite 3.7 6 0.1 109.3

25645 405106 2087683 176 Basaltic agglomerate. Hematite‐stained.

12F 2 Sub‐Propylitic Kaolinite‐smectite 10.3 51 0.1 53.5

25646 405103 2087827 184 Sandstone 1C 2.67 Sub‐Propylitic Kaolinite‐smectite 16.4 17 0.3 151







25650 407226 2089567 301 Quartz‐specularite veinlets 12F 0.21 Argillic Illite 34.7 1 3.3 0.7

25651 407096 2089837 296 Intrusive rock with tourmaline veinlets.

33 Potassic Schorl 4.1 2 0.1 30.9

SAM= sample number, East=easting, North=northing (UTM co‐ordinates, NAD27 datum), ELEV=elevation in meters, LITH= lithology code (see Fig. X for explanation of lithology codes), MAG=magnetic susceptibility in SI units, ALT. ASSEM. = alteration mineral assemblage, ALT. MIN. = alteration mineral identified with Terraspec SWIR spectrometer, ppm = parts per million, ppb = parts per billion, Cu = copper, Zn = zinc, Ag = silver, Au = gold. Original file is EVR_ROCKS.xlsx.



Appendix 2: Abbreviated listing of Core Samples HoleID FRM TO SAM COMMENT LITH MAG ALT. ASSEM. ALT. MIN. Ba

ppm Zn ppm

Cu ppm

K% Al%

Si% S%

APV04‐08

54 56 36482 Pink pyrophyllite domains, red hematite domains.

50W 0.18 Advanced Argillic

Pyrophyllite 188 43 5 1.2 10.6

30.0

0.4

APV04‐08

112 114 36211 Schist. Tan domains and maroon, hematized domains.

50W ‐0.17 Advanced Argillic

Pyrophyllite 265 5 72 0.2 1.9 11.3 2.9

APV04‐08

130 132 36220 Schist. Pale blue (altered cordierite??) domains and pyritic domains.

50W 1.48 Argillic Kaolinite 291 5 5 0.6 7.8 14.3 11.0

APV04‐08

156 158 36233 Schist. Hard, pink domains. Cross cut by thin veinlets of white clay, red specularite and minor pyrite.


Pyrophyllite 121 48 5 0.1 4.7 38.2

1.0

APV04‐08

162 164 36236 Schist. Hard, pink domains. Cross cut by thin veinlets of white clay.


Pyrophyllite 173 125 60 0.2 5.5 36.0

0.4

APV04‐08

168 170 36239 Pink rock that consists of cryptocrystalline cherty quartz and network‐textured crystalline specularite.

LC 0.17 125 93 41 0.1 1.1 46.4

0.3

APV04‐08

176 178 36243 Massive finely crystalline, dirty pyrite.

LC 0.23 274 5 150 0.1 1.3 29.6

20.9

APV04‐08

180 182 36245 Massive finely crystalline specularite.

LC 0.13 143 5 76 0.1 1.0 38.9

0.7

APV04‐08

186 188 36248 Finely crystalline hematite. Patches of medium crystalline pyrite. Not obvious which is older.

LC 1.61 258 5 224 0.1 0.0 18.4

29.3

APV04‐08

198 200 34854 Pink rock that consists of cryptocrystalline cherty quartz and network‐textured crystalline specularite.

LC 0.41 5 5 44 0.1 1.3 28.2

1.9

APV04‐08

214 216 34862 Pink rock that consists of cryptocrystalline cherty quartz and network‐textured crystalline specularite. Cross‐cut by veinlets of pure kaolinite with cockscomb quartz.

LC 0.36 Argillic Kaolinite 103 5 5 0.1 1.0 51.1 0.4

APV04‐08

220 222 34865 Pink rock that consists of schist and network‐textured crystalline pyrite.

50W 0.3 Argillic Kaolinite 260 5 384 0.1 3.8 36.6

9.1

APV04‐08

226 228 34868 Foliation parallel pinkish pyrophyllite in quartz‐pyrite schist.


Pyrophyllite 918 5 87 0.4 7.7 26.0

4.1

APV04‐08

234 236 34872 Pink rock that consists of cryptocrystalline cherty quartz and network‐textured crystalline specularite with clay veinlets.

LC 0.1 Advanced Argillic

Pyrophyllite 5 5 5 0.1 0.5 30.9

0.5

APV09‐15

11.5 12.6 313205 Rock pervasively replaced by white clay. Limonite in fractures, quartz‐goethite veinlets.

0.43 Argillic Halloysite 207 2286 3107 0.2 2.7 6.8 0.2

APV09‐15

20.5 22 313215 Rock pervasively replaced by white clay. Hematite in fractures. Possible remnants of quartz‐filled amygdules.

0.05 Argillic Halloysite 5 189 106 0.3 3.5 11.6 0.3

APV09‐15

25 26 313219 Brecciated, basaltic rock with greasy white clay on fractures.

12A 3.25 Sub‐Propylitic Montmorillonite 5 248 2478 0.1 9.2 22.0

0.9

APV09‐15

27.35 28.3 313221 Brecciated, basaltic rock with greasy white clay on fractures. Pyritic veinlets with chalcocite coatings.

12A 0.41 Sub‐Propylitic Montmorillonite 165 297 6143 0.3 15.4

19.3 2.4

APV09‐15

35.5 37 313228 Siliceous intrusive rock with propylitic overprint. Tonalite?

21F ‐0.21 Sub‐Propylitic Chlorite 152 38 48 0.1 6.2 35.2 0.1

APV09‐15

44 45 313234 Basaltic rock with quartz‐filled amygdules, quartz pyrite veinlets.

12A 0.58 Sub‐Propylitic Chlorite 262 529 215 1.1 5.7 29.6

9.9

APV09‐15

58 59 313249 Rock pervasively altered to pyrite and possibly bornite. Cannot recognize protolith.

12A 0.33 Quartz 244 741 6221 0.8 6.2 25.7 13.5



HoleID FRM TO SAM COMMENT LITH MAG ALT. ASSEM. ALT. MIN. Ba ppm

Zn ppm

Cu ppm

K% Al%

Si% S%

APV09‐15

64 65 313256 Scoriaceou basaltic fragments replaced by chalcedony. Pyrite and white sphalerite in vugs.

12A 0.1 387 2133 126 1.4 5.4 31.5 7.0

APV09‐15

67 68 313259 Scoriacous basalt. Quartz‐pyrite chlorite alteration.


4.0

APV09‐15

70 71.2 313262 Blackjack sphalerite veins with pyritic selvedges in chlorite‐altered basalt.

12A 0.6 Sub‐Propylitic 346 236707

10941 0.6 7.7 10.0

23.7

APV09‐15

73 74.5 313264 Intense, pervasive chlorite alteration.

12A 0.14 Sub‐Propylitic Chlorite 192 235 5 0.2 2.7 7.1 0.1

APV09‐15

94 95.5 313279 Intense, pervasive epidote and chlorite alteration.

12A 0.34 Propylitic Epidote 184 5 5 0.0 6.8 25.5

0.2

APV10‐02

2.15 3.5 311053 Red, hematite‐altered rock x‐cut by white clay veinlets (no quartz).

0.19 Argillic Kaolinite‐smectite

112 148 1144 0.6 4.2 11.2 0.2

APV10‐02

9.5 10.93 311058 Orange, limonite‐altered rock cross‐cut by white clay veinlets (no quartz)


5 444 1694 0.3 3.4 8.8 0.1

APV10‐02

17.5 18.5 311066 Red, hematite‐altered rock x‐cut by white clay veinlets (no quartz).


165 886 572 0.3 11.2

20.2

0.3

APV10‐02

20.5 21.2 311069 Monzodiorite porphyry with isolated chalcanthite‐stained feldspar phenocrysts in a matrix of sticky grey clay and abundant finely crystalline pyrite.

32PX 0.4 140 1428 31483 0.1 2.9 9.1 3.8

APV10‐02

22 23.15 311071 White‐grey rock with remnant chlorite‐filled amygdules. Pervasive argillic alteration. Cross‐cut by white kaolinite (no quartz) veinlets.

12A 0.1 Argillic 221 836 1897 0.5 3.3 10.4

0.5

APV10‐02

23.15 24 311072 Monzodiorite porphyry with isolated Chalcanthite‐stained feldspar phenocrysts in a matrix of sticky grey clay and abundant finely crystalline pyrite.

32PX ‐0.22 Chalcanthite 277 631 35293 0.2 3.0 7.2 7.1

APV10‐02

24 25 311073 Monzodiorite porphyry with isolated Chalcanthite‐stained feldspar phenocrysts in a matrix of sticky grey clay and abundant finely crystalline pyrite.

32PX 0.57 Chalcanthite 885 302 24438 1.2 4.0 9.5 6.1

APV10‐02

30 31 311081 Monzodiorite porphyry with isolated Chalcanthite‐stained feldspar phenocrysts in a matrix of minor sticky grey clay almost 85% finely crystalline pyrite with a red hematite stain.

32PX 0.09 Chalcanthite 365 765 22951 0.7 3.8 10.5 5.3

APV10‐02

41 42 311093 Monzodiorite porphyry with isolated Chalcanthite‐stained feldspar phenocrysts in a matrix of sticky grey clay and abundant finely crystalline pyrite.

32PX 0.15 157 452 934 0.2 5.3 21.1 8.9

APV10‐02

43 44.5 311096 Monzodiorite porphyry. Clay‐altered, pervasively replaced by pyrite. Chalcocite on pyrite, chalcanthite‐stained feldspar. 10% chalcedonic quartz veins with sphalerite and Au cross‐cut the pyritized porphyritic phenocrysts.

32PX 0.63 Quartz 254 5179 10983 0.7 3.8 9.3 10.6

APV10‐02

49 50.5 311201 Quartz‐feldspar porphyritic rhyolite. Greenish matrix, disseminated pyrite.

10C 0.39 Sub‐Propylitic Illite 173 72 5 0.2 5.3 36.0

0.2

APV10‐02

58 59.5 311207 Quartz‐feldspar porphyritic rhyolite. Tiny chlorite‐altered hornblende. Greenish

10C 0.23 Sub‐Propylitic Illite 299 605 5 0.9 5.0 30.6

0.5




Zn ppm

Cu ppm

K% Al%

Si% S%

matrix, disseminated pyrite.

APV10‐02

64 65.5 311212 QSP rock with greenish chlorite (?) domains.

12A 0.14 Sub‐Propylitic 212 307 122 0.5 1.6 23.6

3.0

APV10‐02

77.5 79 311221 Rock with quartz‐filled amygdules up to 1 cm across. Matrix pervasively pyritized with chlorite.

12A 0.46 Sub‐Propylitic Fe‐chlorite 244 305 5 0.2 4.2 32.5 2.7

APV10‐02

106 107.5 311241 Quartz‐feldspar porphyritic rhyolite. Tiny chlorite‐altered hornblende. Greenish matrix, disseminated pyrite.

10C 0.09 Sub‐Propylitic Fe‐chlorite 197 5 5 0.2 3.7 31.7 0.1

APV10‐03

8.5 9 311249 Feldspar porphyritic andesite. 15% 1‐2 mm feldspar phenocrysts and glomerocrysts. Tiny, chlorite filled amygdules, and some larger quartz‐filled amygdules.

11B 0.5 Sub‐Propylitic Chlorite 203 959 551 0.1 7.5 21.7 0.1

APV10‐03

10 11.5 311251 Massive quartz‐iron rock. Gossan. Not vuggy. Heavy. Dark brown. Ore formed from weathering.

1.1 Goethite 241 1904 10310 0.1 2.6 5.0 0.5

APV10‐03

14.5 19 311254 Mainly skeletal vuggy quartz with minor clay and limonite in vugs.

VS 0.27 Sub‐Propylitic Illite‐smectite 101 5 64 0.1 0.0 42.4

0.1

APV10‐03

20.5 22 311257 White rock of vuggy residual silica. Orange limonite on fractures.

VS 0.09 Quartz 647 5 34 0.1 0.6 43.1 0.2

APV10‐03

22 23.5 311258 Pervasively altered to brown Fe‐oxide. Tiny ovoid amygdules < 1 mm across filled with white clay. No veining.

11B 0.14 Sub‐Propylitic Goethite 375 5 461 0.5 1.9 18.3 0.7

APV10‐03

26.5 28 311261 Residual, vuggy quartz with minor white clay and earthy red hematite.

VS Hematite 874 5 5 0.8 2.4 36.7 0.1

APV10‐03

31 31.5 311264 Orange rock of mainly iron oxide with skeletal vuggy silica.

VS 0.18 Goethite 254 5 267 0.4 0.6 25.3 1.3

APV10‐03

33.5 35.25 311267 Yellow rock of granular quartz with illite and yellow jarosite. Leached.

11B 0.1 Argillic Illite 486 5 5 2.3 5.8 13.2 8.3

APV10‐03

35.25 36.5 311268 Monzodiorite porphyry with isolated Chalcanthite‐stained feldspar phenocrysts in a matrix of sticky grey clay and abudant finely crystalline pyrite.

32PX 0.19 Argillic Kaolinite‐smectite

414 75 31522 2.0 11.0

14.2

11.5

APV10‐03

44 45 311276 Aphyric, amygdaloidal basaltic breccia. Unsorted, probably a hyaloclastite. Breccia matrix replaced by 10% finely crystalline pyrite that is coated by chalcocite. Rock fragments pervasively replaced by alunite as well as hydrated products of alunite (alum).

12AF 0.42 Advanced Argillic

Alum 293 1418 13596 1.3 11.5 17.7 7.6

APV10‐03

51.5 53.5 311282 Mafic Dike. Magnetic. Not altered.

33 18.6 289 1694 136 0.1 7.9 21.9

0.1

APV10‐03

66.5 68 311293 Basaltic Hyaloclastite. Matrix preferentially sulfidized (pyrite) and chloritized.

12AF 0.77 Sub‐Propylitic Illite‐smectite 254 437 371 0.2 8.6 17.4 10.5

APV10‐03

78.5 80 311302 Basalt with white calcite veinlets.

12A 0.35 Sub‐Propylitic Fe‐chlorite 256 90 98 0.2 7.2 24.8

1.5

APV10‐03

80 81.7 311303 Monzodiorite. Zoned feldspar in a chlorite matrix. Disseminated pyrite.

32 0.1 Sub‐Propylitic Fe‐chlorite 234 54 5 0.5 4.1 24.9

0.3

APV10‐04

6.5 8 311318 Brecciated rock. Fragments consist of vuggy silica. Hematite stain.

VS 0.28 Quartz 85 5 96 0.1 0.0 39.2

0.4




Zn ppm

Cu ppm

K% Al%

Si% S%

APV10‐04

17 18.5 311325 Greasy rock with hematite stain.


286 21 144 0.1 6.4 15.8 0.2

APV10‐04

18.5 20 311326 Greasy rock with hematite stain.

0.61 Argillic Montmorillonite 5 172 140 0.1 5.0 14.0

0.3

APV10‐04

20 20.6 311328 Finely crystalline rock. Red. Brecciated. Clay+boxwork after sulfide in veinlets. No quartz veining.

0.28 Sub‐Propylitic Montmorillonite 236 357 2029 0.1 8.3 23.7 0.3

APV10‐06

10.5 11.5 311423 Clastic rock with poorly sorted, subangular fragments up to 4 cm across. From boxwork, sulfides preferentially occur in sandy matrix. Pervasive clay alteration.

1D 0.31 Argillic Kaolinite‐smectite

5 832 1496 0.0 4.6 9.3 0.3

APV10‐06

13.5 14.25 311426 Limonite‐stained, clay‐altered rock

0.55 Sub‐Propylitic Buddingtonite 5 8982 13997 0.1 2.4 8.5 0.4

APV10‐06

14.25 14.65 311427 Rock consists of very soft, greasy, greenish clay (talc/saponite). Rosettes of malachite and azurite (rxn HCL) AND a bronze copper wad.

32PX 0.14 Sub‐Propylitic Malachite 5 6472 35% 0.0 4.9 11.3 0.1

APV10‐06

14.65 15.6 311428 Limonite stained rock. Brecciated, mammillary malachite in fractures. Rock pervasively altered to green clay.

32PX 0.26 Sub‐Propylitic Chlorite 227 21112 14425 0.1 7.0 13.3 0.2

APV10‐06

15.6 17 311429 Red, white and orange stained rock. Protolith indeterminate.

0.36 Sub‐Propylitic Ferrihydrite 5 10623

3861 0.0 3.4 8.2 0.1

APV10‐06

20.8 21.5 311434 Grey rock, hard, partially pervasive clay. 2‐3% disseminated pyrite. Limonite on fractures.

12A 0.33 189 3016 741 0.3 2.9 9.2 1.4

APV10‐06

23.5 24.5 311437 Silicified basalt cross‐cut by coarsely crystalline sphalerite and pyrite in a matrix of white, microcrystalline (not cockscomb) quartz.

12A 0.86 5 414360

22570 0.1 3.1 10.3 23.6

APV10‐06

33.5 35 311447 Quartz‐feldspar porphyritic rhyolite. Matrix pale green.

10C 0.31 Sub‐Propylitic Illite 424 754 5 0.8 5.3 37.5 0.1

APV10‐06

40.5 41.5 311453 Basalt ‐‐ pervasive clay alteration with disseminated pyrite. Cross‐cut by quartz veinlets with disseminated pyrite.

12A 0.51 Sub‐Propylitic Fe‐chlorite 167 1121 5 0.1 4.8 32.2

0.6

APV10‐06

48.5 50 311461 Dark basaltic rock cross‐cut by wormy white calcite veinlets.

12A 0.47 Sub‐Propylitic Fe‐chlorite 211 115 5 0.0 2.7 7.3 0.2

APV10‐06

59 60.5 311469 Maroon, hematitic basalt cross‐cut by wormy white calcite veinlets.

12A 0.45 Sub‐Propylitic 187 89 5 0.1 4.3 10.6

0.1

APV10‐06

104 105 311493 Dark green, chloritized basaltic rock with disseminated pyrite. Cross‐cut by white calcite veinlets.


0.6

APV10‐07 9.5 11 311502 Limonite‐stained, clay‐altered rock

0.35 Sub‐Propylitic Ferrihydrite 5026 349 1173 1.6 2.2 8.5 0.2

APV10‐07 12.5 14 311505 Siliceous rock with round features (amygdules) filled with chalcocite‐coated quartz.

12A 0.13 329 628 6822 1.7 4.9 32.4

6.2

APV10‐07 14 15 311506 Quartz‐pyrite rock with minor bornite.

0.76 528 596 26551 3.2 4.7 12.8

5.4

APV10‐07 17 18 311509 White, siliceous rock with sphalerite‐filled amygdules.

12A 0 Argillic Montmorillonite 672 12467 891 3.4 11.5 28.0

4.3

APV10‐07 20.35 21.5 311513 Greasy, clay altered rock with disseminated euhedral pyrite, sphalerite and minor chalcocite on pyrite. No diagnostic textures for lithological determination.

0.16 Montmorillonite 132 6135 122 1.3 9.0 9.8 7.3

APV10‐07 21.5 22.5 311514 12AF 0.26 Chlorite 151 14022

1276 0.0 7.4 13.9 4.0




Zn ppm

Cu ppm

K% Al%

Si% S%

TBM‐07 6.1 7.62 19641 Quartz‐feldspar porphyritic rhyolite. Altered to tan clay. Weathered.

10C 0.14 Sub‐Propylitic Montmorillonite 5 5 5 0.1 5.4 19.7 0.1

TBM‐07 16.15 16.76 19648 Quartz‐feldspar porphyritic rhyolite. Altered to pale blue‐green clay and pistachio green epidote. Quartz phenocrysts.

10C 0.42 Propylitic Illite‐smectite 93 89 5 0.2 6.2 20.8

0.1

TBM‐07 20.2 21.8 19652 MASSIVE SULFIDE! Mainly sphalerite, bornite, chalcopyrite and barite. Muscovite.

7 0.19 ORE 11504

98913

42546 0.1 2.2 5.3 7.6

TBM‐07 21.8 27.43 19659 MASSIVE SULFIDE! Mainly brown, fine grained sphalerite, minor galena. Cross‐cut by medium crystalline chalcopyrite and bornite.

7 0.01 ORE 4334 51533 21459 0.8 3.3 6.2 9.0

TBM‐07 26.6 27.43 19661 Piece of semi‐massive chlorite from below massive sulfide.

50G 0.23 Chloritic Fe‐Chlorite 265 1357 5 0.1 6.7 19.4

0.5

TBM‐07 45.72 47.24 19668 Siliceous rock with pyrite and minor foliation parallel sericite (possibly after andalusite).

50W 1.42 Sericitic Andalusite 595 5 5 1.1 2.4 32.9

7.0

TBM‐11 21.34 22.86

19737 Quartz‐feldspar porphyritic rhyolite. Altered to tan clay. Weathered.

10C 0.13 Propylitic Epidote 117 5 5 0.6 4.2 16.3 0.0

TBM‐11 22.86 24.38

19738 Quartz‐sericite‐pyrite rock.

50W 0.21 Sericitic Andalusite 531 5 1505 1.5 4.4 12.0

13.4

TBM‐11 32 33.53 19744 Quartz‐chlorite‐pyrite rock.

50G 0.16 Sericite‐chlorite Chlorite 372 5 73 1.1 1.7 22.8

3.8

TBM‐11 33.53 35.05 19745 Pale green sericite‐pyrite rock

50W ‐0.22 Sericitic Muscovite 1134 73 2199 2.4 8.9 19.7 11.1

TBM‐11 38.1 39.62

19748 Pale green sericite‐pyrite‐chlorite rock

50W 0.22 Sericite‐chlorite Muscovite 324 86 5 0.6 1.9 21.1 5.3

TBM‐11 57.91 59.44

19761 White sericite rock 50W 0.12 Sericitic Illite 299 5 5 1.0 4.1 25.0

0.9

TBM‐11 68.58 69.49

19768 Green rock, pervasively altered to chlorite and calcite

12A 0.23 Propylitic Fe‐chlorite 1369 78 5 1.1 5.0 14.8

0.3

CUA‐02 5.8 6.5 167105 White, silky schist with barite and about 20% foliation parallel sulfide ‐‐ mainly sphalerite and pyrite. ORE HORIZON

50W 0.21 Sericitic Andalusite 3259 218931

237 5.0 18.8

20.0

11.1

CUA‐02 18.5 20 167114 Bleached, white rock with disseminated to stringer chalcocite‐stained pyrite. FOOTWALL STOCKWORK. Although rock matrix appears white (oxidized), spectra clearly identify chlorite

50W 0.18 Sericite‐chlorite Chlorite 517 258 35575 1.3 7.3 18.9

22.1

CUA‐02 45.5 47 167132 White schist with foliation parallel quartz‐pyrite veinlets, muscovite domains, grey andalusite domains.

50W 0.5 Sericitic Andalusite 1065 93 42 2.2 6.8 35.7 2.1

CUA‐02 66.5 68 167146 White schist with foliation parallel quartz‐pyrite veinlets, muscovite‐chlorite domains, grey andalusite domains.

50W ‐0.32 Chloritic Andalusite 766 544 37101 1.7 8.0 20.5

20.4

CUA‐02 104 105.5 167171 Green schist with metamorphic segregation of white quartz with chalcopyrite and bright green chlorite. Andalusite domains.

50G 0.25 Chloritic Andalusite 170 305 22786 0.2 3.5 26.1

14.5

CUA‐02 122 123.5 167183 Green schist with metamorphic segregation of clear quartz, bright green chlorite and muscovite. Pyrite, chalcopyrite in foliation parallel domains.

50G 0.38 478 116 9299 1.5 5.8 29.6

9.2




Zn ppm

Cu ppm

K% Al%

Si% S%

CUA‐02 149 150.5 167201 Green schist with foliation parallel segregations of chlorite and andalusite. Pyrite‐chalcopyrite stringers in variable directions, some crossing the foliation.

50G 0.6 Chloritic Andalusite 244 125 35575 0.3 2.9 33.4 11.3

CUA‐03 17 18.5 167220 White, silicified rhyolite fragments (domains) in a soft green phyllosilicate (phengite) matrix

10CFX

0.18 Sericitic Phengite 6523 414 330 3.1 5.9 27.0 0.2

CUA‐03 29 30.5 167227 Schistose rhyolite with foliation parallel, chalcocite‐coated pyrite. Green antlerite (?) oxide.

10CFX

0.82 Sericitic Phengite 6806 1329 36837 2.7 6.1 22.8

3.3

CUA‐03 30.5 32 167228 Schistose rhyolite with bright white phyllic domains and quartz‐rich domains with pyrite, chalcocite, minor chrysocolla.

10CFX

0.67 Sericitic Phengite 5022 1241 31380 4.2 7.7 20.0

4.9

CUA‐03 36.5 38 167232 Green, schistose rhyolite. Disseminated pyrite, chalcocite.

10CFX

1.52 Sericite‐chlorite Chlorite 1466 863 1480 0.9 4.0 35.4 1.1

CUA‐03 42.5 44 167236 White, schistose, silicified rhyolite with about 1.5% disseminated, white sphalerite and minor pyrite.

10CFX

0.2 Sericitic Muscovite 866 2451 716 0.8 1.7 39.1 1.1

CUA‐03 47 48.5 167239 White, schistose, silicified rhyolite with about 1.5% disseminated, white sphalerite and minor pyrite.

10CFX

0.19 Sericitic Muscovite 884 1030 5404 0.8 2.0 38.0

2.1

CUA‐04 15.5 17 167262 Irregular white domains in a matrix of green chlorite‐phengite.

10CFX

0.59 Sericite‐chlorite Phengite 5710 724 476 2.8 7.7 28.0

0.2

CUA‐04 27.5 29 167270 Rock pervasively replaced by white mica. Foliation parallel quartz‐pyrite‐chalcopyrite. Green Cu‐oxide.

50W 0.4 Sericitic Muscovite 6515 333 992 2.9 7.3 29.5

3.5

CUA‐04 44 45.5 167281 White siliceous domains in a matrix of green chlorite. Foliation parallel pyrite, white sphalerite, chalcopyrite, chalcocite.

10CFX

0.27 Chloritic Chlorite ### 1269 1328 0.6 4.6 33.5 3.4

CUA‐04 45.5 47 167282 About 10% foliation parallel white sphalerite with disseminated pyrite, chalcopyrite.

50W 0.45 Sericitic Phengite ### 59746

4206 3.7 10.4

30.1 7.0

CUA‐04 57.5 59 167290 White siliceous domains in a matrix of green chlorite. Minor disseminated pyrite, white sphalerite, chalcopyrite.

10CFX

0.18 Sericite‐chlorite Chlorite 1271 823 437 2.3 6.3 21.4

1.3

CUA‐04 66.5 68 167296 White siliceous domains in a matrix of dark green chlorite. Minor disseminated euhedral pyrite.

10CFX

0.4 Sericite‐chlorite Chlorite 495 88 5 1.6 4.4 30.0

0.3

CUA‐04 71 72 167299 Pale green muscovite with disseminated pyrite, sphalerite veinlets.

50W 0.35 Sericitic Muscovite 491 853 125 1.9 5.8 32.2

0.8

CUA‐04 96.5 98 167322 Pale green rock with domains of dark green chlorite. Minor disseminated euhedral pyrite.

50G 0.08 Chloritic Chlorite 549 589 5 1.4 2.5 24.6

0.8

CUA‐04 134 135.5 167347 Quartz‐epidote chlorite veining in fine‐grained mafic rock

12A 0.9 Propylitic Chlorite 196 5 5 0.1 0.4 28.4

0.1

CUA‐04 146 147.5 168505 Finely crystalline mafic rock with minor quartz‐epidote veinlets. Disseminated magnetite.

12A 8.59 Propylitic Epidote 1949 96 5 4.0 8.8 27.9 0.1

FRM= from, TO=to, SAM= sample number, LITH= lithology code (see Fig. X for explanation of lithology codes), MAG=magnetic susceptibility in SI units, ALT. ASSEM. = alteration mineral assemblage, ALT. MIN. = alteration mineral identified with Terraspec SWIR spectrometer, ppm = parts per million, % = percent, Ba = barium, Cu = copper, Zn = zinc, K= potassium, Al=aluminum, Si=silica, S=sulfur.

Original file is EVR_CORE.xlsx. Geochemical measurements completed on homogenized powders for 75 seconds using a Niton portable XRF GOLDD.

2010_apv

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