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Geology and Petrology of Quaternary Volcanic Rocks, Garibaldi Lake Area, Southwestern British Columbia: Summary

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Geology and Petrology of Quaternary Volcanic Rocks, Garibaldi Lake Area, Southwestern British Columbia: Summary Geology and petrology of Quaternary volcanic rocks, Garibaldi Lake area, southwestern British Columbia: Summary NATHAN L. GREEN" Department of Geological Sciences, University of British Columbia, Vancouver, British Columbia, Canada INTRODUCTION GEOLOGY Subduction of the Juan de Fuca plate beneath the North Ameri- The Garibaldi Lake volcanic suites record at least two periods of can plate has been accompanied by Pleistocene-Holocene eruptions eruptive activity. Hornblende-andesite flows and pyroclastic mate- of basalt, andesite, and dacite along the Garibaldi volcanic belt in rials were erupted during the earliest phase of activity at The Black southwestern British Columbia (Souther, 1977; Keen and Tusk and Mount Price complexes (Fig. 1); the latter (Red Hyndman, 1979). The 25-km-wide belt, comprising at least eigh- Mountain) andesites were extruded onto glacial sediments that teen volcanic complexes, lies approximately 250 km inland from suggest the existence of an earlier continental ice sheet or a local the convergent margin. It extends from Mount Garibaldi, at the alpine glacier. After quiescent periods of unknown length, activity head of Howe Sound, northwesterly for 140 km to Bridge River. was renewed at both centers. Eruption of hypersthene-andesite Volcanism in the Garibaldi Lake area, about 6 km north of Mount lavas, culminating in the extrusion of an endogenous dome, con- Garibaldi, produced a succession of flat-lying olivine basalts in the structed the second-stage cone of The Black Tusk. Hornblende- Cheakamus River valley, basaltic-andesite lavas at The Cinder biotite andesite flows and tuff breccias formed the nearly symmetri- Cone and Sphinx Moraine centers, and a line of three andesitic cal Mount Price cone on the western fllank of the Red Mountain complexes: The Table, Mount Price, and The Black Tusk. volcano. Phreatic eruptions at The Cinder Cone produced a broad TABLE 1. PHENOCRYST EQUILIBRATION TEMPERATURES AND ESTIMATED PRE-ERUPTIVE WATER CONTENTS f melt C B Suite Lithology" Tl" T2 T? PHs0 (bars)" Ptotai (bars)' X» 20 Wt % h2o Cheakamus Valley BSLT 1027 500 1000 0.21 1.0 Desolation Valley BSAT 1025 1024 1090 3900 0.27 2.8 Sphinx Moraine HBST 992 973 2240 5750 0.38 3.6 Table Meadow HADT 939 936 2230 3800 0.43 3.8 Table HADT 909-937 909- 949 2530-2900 3400-3900 0.42-0.47 3.7-5.5 The Black Tusk (Stage II) HYAN 965-982 960-1010 924 1510-1880 2900-3300 0.32-0.39 3.1-3.5 Mount Price/Clinker Peak HBAN 805-875 2980-3930 3500-4000 0.49-0.57 5.5-7.7 Notes: a. BSLT, basalt; BSAT, amphibole-free basaltic andesite; HBST, hornblende-bearing basaltic andesite; HADT, hornblende andesite; HYAN, hypersthene andesite; HBAN, hornblende-biotite andesite. b. Tl: temperatures (°C ± 60°C) calculated using average pyroxene phenocryst compositions and the Wood and Banno (1973) two-pyroxene geothermometer. c. T2: temperatures (°C ± 70°C) calculated using average pyroxene phenocryst compositions and the Wells (1977) two-pyroxene geother- mometer. d. T3: temperatures (°C ± 30°C) calculated using co-existing Fe-Ti oxides (Buddington and Lindsley, 1964). e. Water pressures estimated from the plagioclase geothermometer of Kudo and Weill (1970) and phenocryst equilibration temperatures using the method of Stormer and Carmichael (1970). Plagioclase temperatures, calculated with average plagioclase and bulk rock compositions, approximate low-pressure liquidus temperatures. Calculated water pressures represent maximum values, with estimated uncertainty of ±750 bars. f- Protai and XflJ'o estimated from Fig. 18 and 19 of Burnham and Davis (1974) using temperatures calculated with pyroxene and Fe-Ti oxide geothermometers and PHl0 derived from Kudo-Weill plagioclase thermometer; PH,0 assumed to equal equilibrium water pressure (P™"). Esti- 1 mated uncertainties are ±1000 bars in PXotal and ±0.05 in Xfi'o - g. Maximum pre-eruptive water contents estimated using XS'o' and activity-composition relations in the NaAlSi3Qj —H20 system (Burnham and Davis, 1974). Estimated uncertainties are ±1.0% water. The complete article, of which this is a summary, appears in Part II of the Bulletin, v. 92, no. 10, p. 1359-1470. * Present address: Department of Geology, University of Alabama, University, Alabama 35486. Geological Society of America Bulletin, Part I, v. 92, p. 697-702, 2 figs., 2 tables, October 1981. 697 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/92/10/697/3429817/i0016-7606-92-10-697.pdf by guest on 25 September 2021 PLEISTOCENE - RECENT VOLCANIC ROCKS OF THE GARIBALDI LAKE AREA CLINKER PEAK CHEAKAMUS, QC Hornblende-biotite andesite flows and scoria: a - VALLEY Barrier andesite; b - Culliton Creek andesite. PRICE BAY CONE QPP Hornblende-biotite andesite aggultinate breccia; minor dykes. CHEAKAMUS VALLEY Qv Olivine basalt. THE CINDER CONE QH Helm Creek alkali basalt and mugearite flows; minor pyroclastic material. THE BLACK THE TABLE ,QB* 0.04O /THE c|NDER QTV Table hornblende andesite flows and tuff breccia. o> QoW/jcohJE ÛTm Table Meadow hornblende andesite flow. 13 QBA MOUNT PRICE *Easf Bluff QMb Hornblende-biotite andesite flows. Helm J Glacier QMa Hornblende andesite flows and tuff breccias; minor hornblende-biotite daclte flows and welded tuff. THE CINDER CONE QD Desolation Valley basaltic andesite flow and related pyroclastic material. SPHINX SPHINX MORAINE MORAINE Qs Hornblende-bearing basaltic andesite flow. THE BLACK TUSK A NL MOU Stage II: hvpersthene andesite flows and plug dome. RED MOUNTAIN CONE ÛMr Hornblende andesite flows and tuff breccias. QMg Basal agglomerate; glacial outwash and minor tuffs» THE BLACK TUSK Qßa Stage I: platy pyroxene andesite and hornblende dacite flows, dykes and lithic tuffs. Figure 1. Distribution of Pliestocene-Holocene volcanic rocks in the Garibaldi Lake area. Rock units shown in legend are listed in sequence o 1.2 K-Ar date in millions of years. of eruptive activity inferred from field relations and K-Ar dates Levee. (J. Harakal, 1976, personal commun.). I 2 3 »«""' Pressure ridges. KILOMETERS © Vent. Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/92/10/697/3429817/i0016-7606-92-10-697.pdf by guest on 25 September 2021 GEOLOGY OF GARIBALDI LAKE AREA, SUMMARY 699 TABLE 2. COMPARATIVE CHEMISTRY OF PLEISTOCENE-RECENT VOLCANIC SUITES FROM GARIBALDI LAKE AREA Cheakamus Valley (25) Desolation Valley (4) Sphinx Moraine (3) Range Mean Range Mean gdms§ Range*'1 Mean gdms§ Si02 48.57-52.13 50.08 55.38-56.45 55.99 60.35 54.58-54.96 55.06 64.60 Ti02 1.44- 1.59 1.52 0.84- 0.98 0.94 1.28 0.87- 0.89 0.88 0.81 AI2O3 15.08-16.31 15.73 16.85-18.04 17.33 18.01 17.29-17.40 17.42 18.76 Fe203* 10.02-12.32 11.28 6.95- 7.75 7.44 5.71 6.71- 6.76 6.76 2.38 MnO 0.13- 0.16 0.13 0.12- 0.14 0.13 0.11 0.10 0.10 0.03 MgO 6.42- 8.81 8.43 4.84- 5.46 5.21 2.12 5.80- 6.73 6.31 1.48 CaO 8.47- 9.00 8.64 6.78- 7.11 6.97 6.01 8.05- 8.25 8.14 5.29 Na20 2.77- 4.14 3.47 4.18- 4.77 4.51 4.97 3.70- 3.98 3.84 4.69 K2O 0.38- 0.63 0.47 0.99- 1.14 1.06 1.43 1.09- 1.18 1.14 1.95 P2O5 0.25- 0.33 0.28 0.40- 0.41 0.41 0.31 0.31 Nb 9- 12 11 3- 12 9 5 5 Y 18- 23 21 20- 27 23 22 22 Zr 90-109 102 88-141 118 124 124 Rb 4- 9 7 9- 12 10 13 13 Sr 448-559 467 752-964 774 1300-1309 1306 Ba 80-163 132 305-462 356 462 462 Cu 47- 60 57 38- 51 43 56 56 Zn 93-115 107 79- 84 82 55 55 Ni 69-147 118 72- 95 83 89- 111 100 Cr 141-192 172 105-104 118 104- 135 120 V 176-228 196 120-163 146 141- 174 158 K/Rb 470-987 774 809-934 872 688-754 716 Note: Total iron reported as Fe^j. ""t Single values indicated two analyses. § Determined by wide-scan microprobe analysis. tuff ring. During the late stages of The Cinder Cone activity, the spinellid, magnesian olivine (Fo87-84), aluminous (4.24% A1203) associated Desolation Valley basaltic andesite spread northward bronzite, diopsidic augite, pargasitic hornblende, plagioclase, and within the glacial valley. The Sphinx Moraine basaltic andesite is- magnetite. The amphibole formed through reaction of earlier- sued from a now-concealed vent near the eastern shore of Garibaldi crystallized olivine with the enclosing andesitic melt. In the Desola- Lake, and olivine basalts were extruded into the glacially scoured tion Valley basaltic andesite, the order of crystallization inferred floor of the Cheakamus River valley. from crystal clots was: spinellid, then olivine, followed closely by The latest phase of volcanism commenced during the last major plagioclase, clinopyroxene, and orthopyroxene. These pétro- (Fraser) continental glaciation. The Table, a hornblende-andesite graphie observations argue strongly against an interpretation that tuya, formed when lava repeatedly flooded a deep, cylindrical pipe the basaltic andesites represent primary magmas. thawed through the ice sheet (Mathews, 1951). After evacuation of (3) The Desolation Valley basaltic andesite contains titano- the continental glacier from higher elevations, the small Price Bay magnetite as inclusions within olivine xenocrysts and as isolated adventive cone was constructed on the northern flank of Mount microphenocrysts. The included grains are enriched in Al, Mg, and Price, and two hornblende-biotite andesite flows were emitted from Cr, and depleted in Ti, Fe, and Mn, compared with the mic- Clinker Peak, a breached lava ring in the western shoulder of rophenocrysts.
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