The Daisie occurrence consists of skarn-hosted copper, molybdenum, zinc and tungsten mineralization. It is located on the southeast side of the northeast-trending Deschamps Creek Valley, which drains into Franklyn Arm of Chilko Lake. The mineralization was discovered in the 1920's, and was worked on in the 1950's and 1960's, and particularly between 1974 and 1980.
The area lies in the Stikinia Terrane and is situated between an important northwest-striking fault, the Stikelan fault, to the northeast, and the Early Tertiary Tiedemann pluton of the Jurassic to Tertiary Coast Plutonic Complex to the south (Geological Survey of Canada Open File 1163, Map 1713A; Bulletin 81).
The Deschamps Valley is underlain mainly by a block of Upper Triassic rocks, bounded on each side of the valley by northeast-striking, steeply-dipping faults. To the southeast and northwest of the faults are Lower Cretaceous rocks, which apparently indicates that the Upper Triassic rocks are an up-thrown block, despite being topographically lower (Bulletin 81). The rocks in the valley are intruded by granodiorite and dioritic stocks, probably related to the Coast Plutonic Complex.
The Daisie mineralization is related to skarn alteration and contact metamorphism that resulted from the intrusion of a hornblende granodiorite stock into the Upper Triassic sequence of volcanic and sedimentary rocks. The volcanics include andesitic to basaltic tuffs, breccias and feldspar porphyry flows. Interbedded with these are limestone, argillites and greywacke. Bedding strikes northeast and dips moderately to steeply northwest (Assessment Report 7574). Northwest-trending, mafic or lamprophyre dykes are also present. The hornblende granodiorite is elongate east-west, measuring about 2 by 1 kilometres. Diamond drilling indicates that other, unexposed intrusive bodies of diorite to granodiorite are present in the area (Bulletin 81).
The intrusions hornfelsed and altered the country rocks; the main granodiorite intrusion is itself altered. The main alteration aureole is about 1 kilometre wide. Locally the distinction between volcanic and clastic sedimentary protoliths is difficult because of the hornfelsing. Biotite is a common alteration product. Also, chlorite and epidote hydrothermal alteration, and silicification and sericitization are present locally, commonly accompanied by disseminated pyrite and pyrrhotite. Gossanous alteration at intrusive contacts is common.
Limestone, interbedded with metavolcanics and metasediments, is recrystallized to a massive, grey or white, sucrosic marble. Relict bedding may be indicated by streaks of biotite. Lenses of hornfelsed mudstone or siltstone also occur in the marble and may contain andalusite. The marble units may be up to 100 metres thick. Of importance is the accompanying skarn alteration of the marble: calc-silicate minerals present include epidote, clinozoisite, grossularite to andradite garnet, diopside, wollastonite, actinolite, calcite, chlorite, apatite and sphene. Veins of these minerals or quartz cut most lithologies. Metavolcanics also have skarn alteration locally. Details of the skarn sequence and petrographic descriptions are given in Assessment Report 8295.
Mineralization on the Daisie claims occurs in a northeast- trending, 800-metre long, 60 to 120-metre wide belt of marble and skarn, immediately south of the contact with the granodiorite stock (Assessment Reports 5712, 7574). The marble band is bounded by metavolcanics, and includes a few small, altered dioritic intrusions. The mineralization is exposed in a series of trenches and cuts on the claims. It may be concordant or discordant, following either bedding planes in the marble or crosscutting fractures; stronger mineralization is associated with the latter (Fieldwork 1986). Commonly, mineralization comprises disseminations or pods of massive sulphides consisting of variable amounts of chalcopyrite, pyrite, pyrrhotite, arsenopyrite, bornite, molybdenite and scheelite. In addition, veinlets of chalcopyrite and pyrrhotite occur in strongly silicified zones, partly oxidized to limonite. There are also quartz-molybdenite veins (Property File - Renshaw, 1975). Minor amounts of sphalerite and galena are common; malachite and azurite occur on fracture surfaces.
Four samples collected from massive sulphide pods and skarn mineralization yielded anomalous values of copper, zinc, molybdenum and silver (Bulletin 81). Samples ranged from 1.7 to 5.1 per cent copper, 0.14 to 0.76 per cent zinc, up to 0.5 per cent tungsten, and 30 to 80 grams per tonne silver (Bulletin 81). No significant gold values are reported. Notable results from earlier work include a sample analysed at 15.6 per cent copper, 117 grams per tonne silver and 1.8 grams per tonne gold (Assessment Report 5712). Drill core results include assays of 0.97 per cent molybdenum and 1.2 per cent tungsten (Assessment Report 7156).
Between 1978 and 1980, 1200 metres of diamond drilling was completed in 29 holes (Assessment Reports 7156, 7574, 8682). Some fairly long intersections of low-grade mineralization were encountered: for example, 0.416 per cent copper over 39.6 metres, 0.32 per cent molybdenum over 15 metres, and 0.3 per cent tungsten over 55 metres (Assessment Reports 7156, 8682).
Overall, however, skarn alteration in the area is irregular and thin, and associated mineralization is erratic in significance.