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Mica Granites of the Kern Mountains Pluton, Eastern White Pine County, Nevada: Remobilized Basement of the Cordilleran Miogeosyncline?

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Mica Granites of the Kern Mountains Pluton, Eastern White Pine County, Nevada: Remobilized Basement of the Cordilleran Miogeosyncline? Mica Granites of the Kern Mountains Pluton, Eastern White Pine County, Nevada: Remobilized Basement of the Cordilleran Miogeosyncline? M. G. BEST Department of Geology, Brigbam Young University, Provo, Utah 84601 RICHARD LEE ARMSTRONG*] Department of Geology and Geophysics, Yale University, New Haven, Connecticut 06520 WILLIAM C. GRAUSTEIN GLENN F. EMBREE Department of Geology, Ricks College, Rexburg, Idaho 83440 ROBERT C. AHLBORN Exxon ComDany, Midland, Texas 79701 ABSTRACT tation is that the final emplacement of the Mesozoic Sevier orogenic belt is exposed Tungstonia body occurred 60 m.y. ago and (Armstrong, 1968a, 1968b; Armstrong and Among the many granitic plutons within that the Skinner Canyon intrusion occurred Hansen, 1966). Here, older rocks of the the Basin and Range province of western between 30 and 45 m.y. ago. The data Cordilleran miogeosyncline are more in- North America, those in the Kern Moun- prompt the conclusion that the magmas tensely metamorphosed and deformed than tains of eastern Nevada and western Utah represent remobilized sialic basement rocks of equivalent age on either side, but are unusual structurally, mineralogically, whose model dates (assuming an initial the intensity of regional metamorphism is and chemically. The two largest intrusions, ratio typical for mantle-derived magmas) variable, both across and along regional which together are exposed over an area of are in excess of 1.5 b.y. strike. 130 sq km (51 sq mi), have well-defined The occurrence of such anatectic intru- border facies of leucocratic and generally sions within the relatively intensely aplitic rocks, or of protoclastic rock de- metamorphosed parts of the infrastructure veloped from coarser core-facies material. of the Sevier orogenic belt, rather than Within the core facies are abundant aplitic, elsewhere in the Basin and Range province, leucocratic dikes. The core facies of the is not unexpected, and it possibly represents larger intrusion (Tungstonia Granite) is a a more advanced evolutionary stage than two-mica granite with conspicuous pheno- do the gneiss domes previously documented crystic books of muscovite up to 5 cm within this same belt. Key words: igneous across. The smaller intrusion (Skinner Can- petrology, muscovite granite, Mesozoic, Sr yon Granite) lacks muscovite, and Fe-Ti isotopes, anatexis. oxides and sphene are constant accessory phases in it. INTRODUCTION Rb-Sr and K-Ar isotopic analyses suggest The Kern Mountains ,(Nelson, 1966, 87 86 a wide range of initial Sr /Sr ratios, which 1969; Best, 1969) lie within a for the most part are unusually high—to north-northeast-trending belt in the eastern nearly 0.7246 for the Tungstonia Great Basin. Here, late Precambrian and Granite—and a complex, protracted period Paleozoic sedimentary rocks were re- of magmatism and isotopic adjustment that gionally deformed and metamorphosed to extended from possibly Mesozoic into greenschist-amphibolite-facies conditions mid-Cenozoic time. The simplest interpre- during Mesozoic time (Misch and Hazzard, 1962), and both synkinematically and postkinematically intruded by granitic plu- Figure 1. Location of Kern Mountains within Present address: Department of Geological Sci- north-northeast-trending belt of mountain ranges (stip- ences, University of British Columbia, Vancouver 8, tons. In this belt (Fig. 1), infrastructure that pled) composed of regionally metamorphosed Precam- Canada. formed within the hinterland of the late brian and Paleozoic rocks in eastern Great Basin. Geological Society of America Bulletin, v. 85, p. 1277-1286, 6 figs., August 1974 1277 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/85/8/1277/3418508/i0016-7606-85-8-1277.pdf by guest on 03 October 2021 1278 BEST AND OTHERS Figure 2. Generalized geologic map of Kern Mountains. Interpretive section along major axis of Kern Mountains pluton has x3 vertical exaggera- tion. The voluminous mica-bearing granites in and forming one large embayment near its gneiss, mica schist, and quartzite. Prepluton the composite Kern Mountains pluton, center, are metamorphosed Paleozoic and mafic dioritic rocks have been cataclasti- which is intimately involved with possibly some late Precambrian rocks dis- cally deformed, recrystallized, and locally metamorphosed miogeosynclinal strata, are playing strong tectonite fabric whose silicified in the Pleasant Valley area of the unusual mineralogically and appear to have geometry is consistent with forceful em- metamorphic envelope. Dioritic sills are exceedingly high and variable initial placement of the pluton (R. C. Ahlborn, folded. Mineralization in and around the Sr87/Sr80 ratios. unpub. data). This metamo-phic envelope pluton it relatively insignificant. The composite pluton (Sayeed, 1972; is, in turn, locally overlain by slices of un- According to Sayeed (1972; also Sayeed Sayeed and others, 1973) is exposed over metamorphosed but brecciated Paleozoic and others, 1973), who has also mapped a double-lobed, northwest-southeast— rocks emplaced by very low angle faulting the pluton as a basis for a geochemical trending area of about 130 sq km (51 sq mi) that postdates plutonism. The metamorphic study, there are three separate intrusions in and forms the core of the Kern Mountains rocks are dominantly marble and dolomitic the range. These are more or less coincident (Fig. 2). Around the margin of the range, marble, with lesser amounts of calc-silicate with those we delineated in our mapping in Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/85/8/1277/3418508/i0016-7606-85-8-1277.pdf by guest on 03 October 2021 MICA GRANITES, KERN MOUNTAINS PLUTON, NEVADA 1279 TABLE 1. CHEMICAL COMPOSITION OF SELECTED MEMBERS OF THE KERN MOUNTAINS PLUTON Sample no.* 8 9AB 9B 40 49 IIB D3 Si02 73.62 74.30 73.19 71.94 73.95 76.38 51.2 Ti02 0.20 0. 05 0.04 0.31 0.25 0.09 1.7 AI2O3 14.26 14.65 14.43 15.86 13.35 12.56 15.3 Fe203 0.15 0.30 0.28 0.33 0.83 0.53 FeO 1.62 0.57 0.83 0.52 0.81 0.54 6.8 MnO 0.03 0.04 0.16 0.00 0.04 0.05 MgO 0.06 C.N 0.39 0.72 0.26 0.04 11.9 CaO 1.93 0.64 0.54 0.19 1.30 0.58 9.2 Na20 3.51 4.00 4.56 2.02 2.88 4.25 2.7 K2O 3.15 4.19 5.04 6.02 5.40 4.01 1.7 + H2O 0.93 0.80 0.38 1.71 0.51 0.65 H2O- 0.05 0.02 0.02 0.08 0.09 0.19 0.05 0.05 0.04 0.02 0.04 0.00 0.2 P2°5 Total 99.56 99. 72 99.90 99.72 99.71 99.86 100.7 Q 35.99 33.29 24.63 35.45 33.59 34.43 0.0 Or 18.37 24.49 30.06 35.63 31 .73 23.94 10.0 Ab 29.84 34.02 38.73 17.27 24.08 36.12 23.0 An 8.95 2.71 2.44 0.81 5.97 2.71 23.8 C 1.73 2.55 0.51 5.71 0.61 0.10 0.0 Di 0.00 0.00 0.00 0.00 0.00 0.00 15.8 Hy 2.61 1.09 2.58 1.93 1.13 0.76 9.6 01 0.00 0.00 0.00 0.00 0.00 0.00 9.2 11 0.46 0.15 0.00 0.61 0.46 0.15 3.2 Mt 0.23 0.46 0.46 0.46 1.16 0.69 5.6 Ap 0.15 0.15 0.11 0.03 0.11 0.00 0.4 * 8. Tungstcnia core fades; fresh sample collected from mine workings in Tungstonia Canyon. K. Aoki, analyst. 9AB. Somewhat pegmatitic Muscovite aplite dike in Tungstcnia core. K. Aoki, analyst. 9B. Garnetiferous Muscovite aplite from border of Tungstonia intrusion in Mallory Canyon. K. Aoki, analyst. 40. Aphanitic sill with phenocrysts of muscovitef feldspar, and quartz. K. Aoki, analyst. 49. Skinner Canyon core fades; fresh sample obtained by diamond core drilling. K. Aoki, analyst. 11B. Skinner Canyon border fades in Pete Neese Canyon. K. Aoki, analyst. D3. Amphibole-rich rock on divide between Rock Springs and Tungstonia Canyons. Analyses by Best on fused whole-rock glass utilizing electron microprobe (see Rucklidge and others, 1970). Total iron cited as FeO in analysis, equally divided in the norm. conjunction with Brigham Young Univer- outward at high angles are everywhere facies of the intrusion. There are many local sity Field Camps from 1967 through 1972. sharp, free of irregularities in form, and pockets less than 1 m across, in which half concordant to foliation in the metamorphic the rock is composed of the books in ran- ROCK UNITS country rocks. Inclusions of country rock in dom array. Euhedral phenocrysts of the intrusion are conspicuously lacking; creamy-white microcline perthite 3 to 4 cm Tungstonia Granite offshoots of granite into the country rock long are sparse. The texture of the rock is The Tungstonia Granite is the .argest of are virtually nonexistent. generally allotriomorphic to somewhat the intrusions; it forms the entire northwest The interior, or core facies, of the Tung- hypidiomorphic and seriate. Grain size lobe of the pluton (Fig. 2). The name is stonia Granite is a relatively uniform ranges more or less continuously from taken from the canyon and from now muscovite-biotite granite, in which plagio- submillimeter up to the size of the perthite abandoned mine workings of the same clase is dominant over perthite (Tables 1, phenocrysts. The seriate material is com- name.1 Typically, the rock is exposed as 2). Among its most striking aspects are posed of quartz, slightly zoned oligoclase castlelike monoliths created by differential large pseudohexagonal books of muscovite commonly containing granules of epidote deep weathering.
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