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Late Cretaceous and Early Tertiary Plutonism and Deformation in the Skagit Gneiss Complex, North Cascade Range, Washington and British Columbia

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Late Cretaceous and Early Tertiary Plutonism and Deformation in the Skagit Gneiss Complex, North Cascade Range, Washington and British Columbia Late Cretaceous and early Tertiary plutonism and deformation in the Skagit Gneiss Complex, North Cascade Range, Washington and British Columbia RALPH A. HAUGERUD U.S. Geological Survey at Department of Geological Sciences, AJ-20, University of Washington, Seattle, Washington 98195 PETER VAN DER HEYDEN* Department of Geological Sciences, University ofBritish Columbia, Vancouver, British Columbia V6T2B4 Canada ROWLAND W. TABOR 1 ,, c „ . , c „ . „ , „ ,., . „.„„ ..„.. „ T,„v \ U.S. Geological Survey, Menlo Park, California 94025 JOHN o. SIALti ) ROBERT E. ZARTMAN U.S. Geological Survey, Denver, Colorado 80225 ABSTRACT The Skagit Gneiss Complex forms a more-or-less continuous ter- others, 1987a, 1987b, 1989). In the core of the range, in what appear to rane within the northern, more deeply eroded part of the North Cas- have been the most deep-seated rocks, direct evidence for the protolith age cade Range. The complex comprises abundant plutons intruded at and age(s) of metamorphism, migmatization, and deformation has been mid-crustal depths into a variety of metamorphosed supracrustal scarce. Relations of gneisses in the northern part of the Chelan block—the rocks of both oceanic and volcanic-arc origin. A plethora of syntec- region bounded by the Straight Creek, Ross Lake, and Entiat faults (Fig. tonic pegmatite, small plutons, and granitic dikes gives the complex a 1)—to surrounding less-metamorphosed rocks have been problematic (for migmatitic aspect. example, Davis and others, 1978; Hamilton, 1978; Whitney and U-Pb zircon ages from gneissic plutons within and near the McGroder, 1989). Skagit Gneiss Complex indicate magmatic crystallization between 75 These gneisses are a complex of metamorphosed granitoid plutons and 60 Ma. Deformation, recrystallization, and migmatization in part with intimately related metamorphosed nongranitoid rocks. Parts of the postdate intrusion of the 75-60 Ma plutons. This latest Cretaceous and complex have been known as the "Custer Granite-gneiss" (Daly, 1912), earliest Tertiary plutonism and migmatization may reflect thermal re- "Custer Gneiss" (McTaggart and Thompson, 1967), and "Skagit Gneiss" laxation following early Late Cretaceous orogeny documented else- (Misch, 1952,1966). We herein adopt the name "Skagit Gneiss," revise it where in the North Cascades. to "Skagit Gneiss Complex," and extend its geographic scope (see Nomen- The complex was ductilely extended northwest-southeast shortly clature, App. A, and Fig. 2).1 after intrusion of granite dikes at -45 Ma, but before emplacement of As part of a restudy of the Custer Ridge area mapped by Daly the earliest (~34 Ma) plutons of the Cascade arc. Outcrops of Late (Haugerud, 1985) and reconnaissance mapping of the North Cascades Cretaceous and earliest Tertiary plutons, migmatites of the Skagit south of the 49th parallel (Tabor and others, 1987a, 1988, and work in Gneiss Complex, and rocks with young ductile deformation are progress), we have obtained U-Pb ages from several plutons within and roughly coextensive, all apparently marking a region of greater middle adjacent to the Skagit Gneiss Complex. Our mapping and these ages lead Eocene unroofing. Unroofing was apparently contemporaneous with us to believe that the magmatic component of the Skagit is largely of latest east-west extension in the Okanogan region to the east and north- Cretaceous and earliest Tertiary age, and that differences between the south and northwest-southeast strike-slip faulting within the North Skagit and surrounding rocks reflect latest Cretaceous and early Tertiary Cascades. deformation and recrystallization and subsequent differential unroofing. In this paper, we (1) outline the geology of the Skagit Gneiss Complex and INTRODUCTION the plutons that we have dated, (2) present and discuss our new U-Pb analyses, and (3) discuss the age of Skagit metamorphism; the significance An early Late Cretaceous age for plutonism and regional metamor- of latest Cretaceous and earliest Tertiary magmas in the North Cascades; phism in much of the North Cascades of northwest Washington and and the age, extent, and tectonic setting of post-45 Ma ductile deformation southwest British Columbia has been well documented and extensively in the Skagit Gneiss Complex. discussed (Mattinson, 1972; McTaggart, 1970; Evans and Berti, 1986; Plummer, 1980; Monger and others, 1982; Haugerud, 1987; Tabor and 'Figure 2 is a folded insert in this issue. Appendices A-C are available free of 'Present address: Geological Survey of Canada, Vancouver, British Columbia charge by requesting Supplementary Data 9125 from the GSA Documents V6B 1R8 Canada. Secretary. Additional material for this article (appendices) is available free of charge by requesting Supplementary Data 9125 from the GSA Documents Secretary. Geological Society of America Bulletin, v. 103, p. 1297-1307, 9 figs., 1 table, October 1991. 1297 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/103/10/1297/3380912/i0016-7606-103-10-1297.pdf by guest on 25 September 2021 CANADA \ 50 km 50° USA 25 miles \ area of figure SB • Vancouver 49° BRITISH COLUMBIA WASHINGTON H3 Pa 48° EXPLANATION H Eocene strata 47° - Q Crystalline rocks i i 123° 122° 120° Figure 1. Sketch map of the North Cascade Range, showing distribution of crystalline rocks, major early Tertiary fault zones, and some localities discussed in the text. Oligocene and younger rocks omitted. The Skagit Gneiss Complex crops out in northwestern part of the Chelan block. Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/103/10/1297/3380912/i0016-7606-103-10-1297.pdf by guest on 25 September 2021 PLUTONISM AND DEFORMATION, SKAGIT GNEISS COMPLEX, NORTH CASCADES 1299 GEOLOGY OF THE SKAGIT GNEISS COMPLEX deformation at lower temperature or higher strain rate. This later deforma- tion is associated with a northwest-trending subhorizontal stretching line- The North Cascade Range lies at the southern end of the Coast ation that is defined by elongate mineral grains and aggregates and is Mountains and at the northern margin of the post-Eocene volcanic rocks commonly more pronounced than is foliation. of the Columbia Embayment. The range constitutes the first extensive Foliations strike northwest and are steep throughout much of the exposure of pre-Tertiary rocks north of the Blue Mountains province of Skagit Gneiss Complex. Large, gently plunging folds of foliation and litho- northeast Oregon. Geology of the North Cascades was summarized by logic layering with steep axial planes are subparallel to a northwest- Misch (1966, 1977,1988) and by Tabor and others (1989). trending stretching lineation. At a few locations along the east and west Eocene faults divide the North Cascades into three belts (Figs. 1 and margins of the Skagit, foliation and lineation strike and trend to the north 2): a western belt of Paleozoic and Mesozoic, mostly oceanic and island- and northeast. The origin of this discordance is unknown. arc-derived strata, commonly overprinted by high-pressure, very low- grade metamorphism; a central core of strongly metamorphosed schist and Maselpanik Area, Northeast Margin of Skagit Gneiss Complex gneiss; and an eastern belt composed largely of unmetamorphosed Jurassic and Cretaceous strata. Many workers (for example, Misch, 1966; Skagit Gneiss Complex in the Maselpanik area (Fig. 2) consists of McGroder, 1989) considered the metamorphic core to be infrastructure to compositionally diverse paragneiss; orthogneiss, including the migmatitic the Late Cretaceous orogen that is recorded in the belts to the east and biotite-hornblende tonalite orthogneiss of Custer Ridge (see App. A, No- west. menclature); and dikes, sills, and a small plug of crosscutting, yet deformed The range is intruded by a suite of ~ 85 to -100 Ma tonalite and granite (Haugerud, 1985). Enstatite in metamorphosed ultramafic rocks granodiorite (Tabor and others, 1989). In the metamorphic core, most of indicates that peak-metamorphic temperatures were >680 °C, assuming a these plutons are deep-seated gneissic bodies at grade with their wall rocks. water-rich fluid phase. Many of the ~85 to ~ 100 Ma plutons are deformed, and radiometric ages Crosscutting relations demonstrate three deformational phases (Fig. from them are among the evidence for Late Cretaceous orogeny. 3). Foliation within amphibolitic xenoliths in the orthogneiss of Custer The metamorphic core is divided into two blocks by the Entiat fault. Ridge represents the earliest event. Subsequent deformation formed the Southwest of the Entiat fault, in the Wenatchee block (Fig. 1), radiometric main foliation (S2) in the orthogneiss of Custer Ridge and (apparently) in cooling ages are largely Late Cretaceous (Engels and others, 1976; Hau- the remainder of the Skagit. Later deformation (D3) produced fabrics in gerud, 1987; Tabor and others, 1987a, 1988). Northeast of the Entiat fault, dikes and sills of lineated granite that cut S2 (Fig. 3). D3 is marked by a in the Chelan block, radiometric cooling ages—especially to the north— pervasive northwest-trending stretching lineation (L3) and local, steep, are early Tertiary (Engels and others, 1976; Tabor and others, 1987a). The northwest-striking foliation (S3, Fig. 3). D3 fabrics are commonly mylo- Skagit Gneiss Complex forms a northwest-trending belt within the north- nitic; quartz is now in ribbons, biotite is smeared into aggregates of smaller ern part of the Chelan block. grains, and plagioclase is locally fractured and extended. Subsolidus origin Pre-Late Cretaceous
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