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Detrital-Zircon Fission-Track Ages for the ''Hoh Formation'

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Detrital-Zircon Fission-Track Ages for the ''Hoh Formation' Data Repository included at end of document Detrital-zircon ®ssion-track ages for the ``Hoh Formation'': Implications for late Cenozoic evolution of the Cascadia subduction wedge Richard J. Stewart² Department of Earth and Space Sciences, University of Washington, Seattle, Washington 98195-1310, USA Mark T. Brandon³ Department of Geology and Geophysics, Kline Geology Laboratory, Yale University, P.O. Box 208109, New Haven, Connecticut 06520-8109, USA ABSTRACT stones commonly can be used as a proxy for Olympic Mountains, Coastal OSC, Hoh depositional age. Formation, zircon ®ssion-track dating. We report new ®ssion-track (FT) ages for Our zircon FT minimum ages indicate detrital zircons for 34 sandstone samples that the Coastal OSC is made up mainly of INTRODUCTION and 2 volcanic ash beds from the ``Hoh lower Miocene (ca. 24 to 16 Ma) sedimen- Formation,'' exposed along the western side tary rocks. We use these age data, together The Olympic Mountains of northwest of the Olympic Mountains of western with other geologic constraints, to recon- Washington State (Fig. 1) mark the ®rst part Washington State. The ``Hoh Formation'' struct a tectonic history. Sedimentary rocks of the Cascadia forearc to emerge above sea is now formally known as the coastal unit of the Coastal OSC were derived from a level, starting at ca. 15 Ma (Brandon and of the Olympic Structural Complex, or mixed-source region that included an active Vance, 1992; Brandon et al., 1998). Uplift and Coastal OSC for short. About 35 zircons volcanic arc and also older units, including erosion of the forearc high in this area provide were dated per sample. The ®ssion-track Cretaceous metamorphic rocks, probably a deep window into the subduction wedge. Ta- grain-age (FTGA) distributions are all located in the Omineca crystalline belt in bor and Cady (1978a, 1978b) used the infor- strongly discordant; grain ages range from the Canadian Rockies. The upper part of mal name Olympic core for these rocks. Bran- 10 to older than 100 Ma. Low vitrinite- the Clallam Formation, located on the don and Vance (1992) suggested Olympic re¯ectance values, short etch times for the northern side of the Olympic Peninsula, ap- subduction complex. To be consistent with zircons, and a broad range of grain ages pears to be a remnant of the sedimentary Stratigraphic Code (Salvador, 1994), we des- indicate that the zircon FT ages are unreset system that fed the Coastal OSC. The sed- ignate here the formal name Olympic Struc- and thus preserve information about cool- iments that formed the Coastal OSC were tural Complex (OSC). This name is a direct ing events in the source region for these initially deposited seaward of the Cascadia replacement for the previous informal names. sedimentary rocks. Five areas were sampled trench, at water depths of .2000 m. This Following Tabor and Cady (1978a, 1978b), repeatedly and yield similar FTGA distri- debris was deposited seaward of the Cas- the OSC refers to the imbricated assemblage butions, demonstrating that sampling er- cadia trench, at water depths of .2000 m, of turbidite sandstone, siltstone, and lesser ig- rors are not a problem. We show that almost and subsequently accreted beneath the neous rocks that structurally underlie the Cres- all of the samples contain a well-de®ned frontal 50 to 100 km of the wedge. Owing cent terrane and the Calawah and Hurricane young component that was probably de- to continued accretion at the front of the Ridge faults, and their lateral equivalents rived from a contemporaneous active vol- wedge, and erosion of the forearc high in (Figs. 1 and 2). These rocks are mainly Eo- canic source, presumably the adjacent Cas- back of the wedge, these lower Miocene cene to middle Miocene in age, but note there cadia arc. Binomial peak-®tting was used to sediments were moved rearward within the is a small enigmatic slice of Mesozoic rocks estimate the FT minimum age, which is the Cascadia subduction wedge. A simple re- exposed in the northwest corner of the Olym- age of the youngest concordant fraction of lationship based on the cross-sectional area pic Peninsula. The OSC could be extended to zircon FT grain ages in a FTGA distribu- of the wedge and a steady accretion ¯ux in- include all equivalent rocks within the Cas- tion. In most cases, minimum ages are sim- dicates that it would have taken ;22 m.y. cadia subduction wedge, but this is generally ilar to fossil ages where available. This re- for the Coastal OSC to reach its present not done given that the Olympic Mountains sult supports our contention that zircon FT position 140 km landward of the toe of the represent the only exposure of the Cascadia minimum ages from volcaniclastic sand- wedge. This estimate is in good agreement wedge north of the California border. with the unit's early Miocene age. Tabor and Cady (1978a, 1978b) mapped ²E-mail: [email protected]. ®ve informal lithic assemblages within the ³E-mail: [email protected]. Keywords: Cascadia subduction wedge, OSC. Brandon and Vance (1992) reorganized GSA Bulletin; January/February 2004; v. 116; no. 1/2; p. 60±75; DOI 10.1130/B22101.1; 13 ®gures; 3 tables; Data Repository item 2004023. For permission to copy, contact [email protected] 60 q 2004 Geological Society of America ``HOH FORMATION'' AND LATE CENOZOIC EVOLUTION OF CASCADIA SUBDUCTION WEDGE the youngest on-land exposures of accreted rocks in the Cascadia subduction wedge. In this paper, we present new ®ssion-track (FT) ages for detrital zircons from sandstones of the Coastal OSC. This approach was ®rst applied in the Olympics by Brandon and Vance (1992) in their study of the age and origin of the Upper OSC and Lower OSC. Age control is commonly sparse in subduc- tion-complex rocks. The FT method provides a useful approach in that one can date indi- vidual zircon grains. If a sandstone has re- mained relatively cool after deposition (,;200 8C), then the grain ages represent the age of cooling for rocks in the source region from which the zircons were derived. Brandon and Vance (1992) presented preliminary evi- dence indicating that the youngest zircon FT grain ages were derived from contemporane- ous volcanic sources in the active Cascade arc. They proposed that the pooled age of that young group of grain ages, called the FT min- imum age, was a useful proxy for the depo- sitional age of the sandstone. We have three objectives here. The Coastal OSC has many localities well dated by benthic foraminifera. Thus, an important ®rst objec- Figure 1. Index map, showing accreted rocks of the Cascadia subduction wedge, which tive is to compare zircon FT minimum ages includes on-land exposures in the Olympic Mountains (Olympic Structural Complex) and with fossil ages to see if the minimum ages in northern California (False Cape and King Range terranes of the Coastal belt of the are a good proxy for depositional age. The Franciscan Complex). The accreted rocks are structurally overlain by the Coast Range second objective is to use the overall distri- terrane. Solid, northeast-pointing arrow indicates convergence velocity of the Juan de bution of zircon FT grain ages to identify the Fuca plate relative to North America at the latitude of the Olympic Mountains (DeMets source of sediments for the Coastal OSC. We et al., 1990; DeMets and Dixon, 1999). use this information to assess previous sug- gestions that rocks now within the coastal unit are offset, by oblique convergence, from an these units into three larger units. The Upper accretion, and may be a more westerly contin- original accretionary setting in the southern unit is equivalent to the Needles-Graywolf and uation of the Lower unit. This possibility was part of the Cascadia margin (e.g., Davis and Elwha assemblages of Tabor and Cady ®rst suggested by Brandon and Vance (1992) Hyndman, 1989; Aalto et al., 1995, 1998). (1978a). It contains mainly Eocene turbidites and is supported by the new ages presented in The third objective is to use depositional ages and minor pillow basalt, and looks as if it this paper. Following past practice (Brandon to interpret the displacement history of the were derived by structural repetition from the and Vance, 1992; Brandon et al., 1998), we Coastal OSC within the Cascadia wedge, from overlying Crescent terrane, which represents a use the following abbreviated names in our an initial site of accretion at the front of the large thrust-bounded structural lid above the discussion below: Upper OSC, Lower OSC, wedge at a water depth .2000 m to its present OSC. The Lower unit is equivalent to the and Coastal OSC. exposures along the Washington coast. Western Olympic and Grand Valley assem- The Coastal OSC has attracted considerable blages of Tabor and Cady (1978a). It appears TECTONIC OVERVIEW attention over the years, in part because of its to be composed mainly of Oligocene and Mio- spectacular exposure in wave-cut outcrops cene turbidites, derived by accretion from the The Cascadia subduction wedge (Fig. 1) is along the Paci®c Coast of the Olympic Pen- subducting Juan de Fuca plate and its sedi- a doubly vergent wedge (Willett et al., 1993) mentary cover. Basalts are very rare in this insula (Fig. 1). Chaotic mudstone-rich meÂ- formed by 35 m.y. of subduction of the Juan unit. langes, locally present in these exposures, de Fuca plate beneath the Cascadia margin We focus here on the Coastal unit, formerly have been the subject of debate since ®rst de- (Brandon et al., 1998; Willett, 1999; Beau- called the Hoh Formation (Weaver, 1916, scribed by Arnold (1905) and Lupton (1914).
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