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Structural and Stratigraphic Evolution of the Calico Mountains

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Structural and Stratigraphic Evolution of the Calico Mountains Structural and stratigraphic evolution of the Calico Mountains: Implications for early Miocene extension and Neogene transpression in the central Mojave Desert, California John S. Singleton* Phillip B. Gans Department of Earth Science, University of California, Santa Barbara, California 93106, USA ABSTRACT rapid unroofi ng of the central Mojave meta- (the Waterman Hills detachment fault) that morphic core complex, yet extension in the juxtaposes tilted early Miocene volcanic and New geologic mapping, structural data, Calico Mountains is minor and is overprinted sedimentary rocks in the hanging wall against and 40Ar/39Ar geochronology document early by dextral faulting and transpression. variably mylonitized basement rocks in the Miocene sedimentation and volcanism and Calico Member beds north of the Calico footwall. Based on apparent offsets of pre-Ter- Neogene deformation in the Calico Moun- fault are intensely folded into numerous tiary markers, several workers (Glazner et al., tains, located in a complexly deformed region east-west–trending, upright anticlines and 1989; Walker et al., 1990; Martin et al., 1993) of California’s central Mojave Desert. Across synclines that represent 25%–33% (up to proposed that 40–60 km of northeast-directed most of the Calico Mountains, volcaniclastic ~0.5 km) north-south shortening. Folds are normal slip occurred along the Waterman Hills sediments and dacitic rocks of the Pickhan- detached along the base of the Calico Mem- detachment fault. The distribution of exten- dle Formation accumulated rapidly between ber and thrust over the Pickhandle Forma- sion is controversial. Dokka (1989) argued that ca. 19.4 and 19 Ma. Overlying fi ne-grained tion, which dips homoclinally ~15–30°S to regional extension occurred within an east- lacustrine beds (here referred to as the Cal- SE. The geometry and distribution of folds west–trending belt across most of the Mojave ico Member of the Barstow Formation) are are most compatible with localized transpres- Desert region. In contrast, Glazner et al. (2002) bracketed between ca. 19 and 16.9 Ma, and sion between the Calico Member and the suggested that extension was largely confi ned are thus older than the type section of the Pickhandle Formation within a positive to an ~25-km-wide area centered around the Barstow Formation in the Mud Hills. Sev- fl ower structure. Transpressional folding and central Mojave metamorphic core complex. eral 17.1–16.8 Ma calc-alkaline dacite domes faulting in the Calico Mountains postdate the Currently there is no strong consensus on intrude the Calico Member and represent a ca. 17 Ma dacite intrusions and appear to be the precise timing of extension in the central previously unrecognized volcanic episode in largely restricted to the area along the Calico Mojave Desert. A few lines of evidence suggest this region. fault restraining bend. that deformation associated with the central In the southern Calico Mountains, the Cal- Mojave metamorphic core complex occurred ico fault (part of the Eastern California shear Keywords: Calico Mountains, Calico fault, Mo- between ca. 24 and 19 Ma. First, a dacite zone) forms a west-northwest– striking, trans- jave Desert, Barstow Formation, transpression. dike in the Mitchel Range and the Waterman pressional restraining bend with ~3 km of Hills granodiorite are interpreted to have been right-lateral slip and perhaps 1 km of reverse INTRODUCTION emplaced synkinematically into the footwall (north side up) throw distributed on two main of the central Mojave metamorphic core com- fault strands. Part of the Calico fault appears The central Mojave Desert region in south- plex (Walker et al., 1990; Fletcher and Bartley, to have originated as an early Miocene normal ern California records a complex deformation 1994); these intrusions have zircon U-Pb ages of fault that unroofed metavolcanic basement history that includes Cenozoic extension, con- 23.0 ± 0.9 Ma and 21.9 ± 0.8 Ma, respectively rocks in the footwall and created a hanging- traction, and strike-slip faulting. Early Mio- (Walker et al., 1990, 1995). Second, the Pick- wall basin in which Pickhandle Formation cene detachment faulting and extensional basin handle Formation volcanic and sedimentary strata accumulated. This extensional slip development generally preceded transform- rocks in the hanging wall of the central Mojave must have largely ceased prior to deposition dominated tectonics related to the Pacifi c–North metamorphic core complex are interpreted as of the Calico Member, which unconformably American plate boundary, yet the timing, mag- synextensional deposits ranging in age from overlies the Pickhandle Formation north of nitude, and tectonic signifi cance of these dispa- ca. 24 to 19 Ma (Fillmore and Walker, 1996). the Calico fault and directly overlies metavol- rate modes of deformation remain controversial Younger (ca. 17–13 Ma) fi ne-grained lacustrine canic rocks south of the Calico fault. Deposi- (see Glazner et al., 2002, for a review). rocks of the Barstow Formation are considered tion of the Pickhandle Formation and at least The central Mojave metamorphic core postextensional deposits. Thermochronologic part of the Calico Member was coeval with complex exposes a low-angle normal fault data of mylonitic rocks from the Mitchel Range *Present address: Department of Geological Sciences, University of Texas at Austin, Austin, Texas 78712, USA. Geosphere; June 2008; v. 4; no. 3; p. 459–479; doi: 10.1130/GES00143.1; 13 fi gures; 1 table; 1 plate; 1 supplemental fi gure. For permission to copy, contact [email protected] 459 © 2008 Geological Society of America Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/4/3/459/3337602/i1553-040X-4-3-459.pdf by guest on 30 September 2021 Singleton and Gans and Hinkley Hills indicate that the footwall of ley et al., 1990). Several strike-slip faults are plify synextensional deposition and transpres- the central Mojave metamorphic core complex considered to be active now (Jennings, 1994). sion in the central Mojave Desert. underwent rapid cooling (50–100 °C/m.y.) Neogene shortening in the Mojave Desert between ca. 21 and 17.5 Ma (Gans et al., 2005). region has primarily been attributed to local GEOLOGIC OVERVIEW OF THE This episode of cooling is interpreted to refl ect transpression along northwest-striking dextral CALICO MOUNTAINS exhumation of the footwall during slip on the faults (e.g., Dibblee, 1980b, 1994), or regional Waterman Hills detachment fault. north-south contraction (Bartley et al., 1990; Located ~15 km northeast of Barstow, the Cal- Strike-slip faulting associated with the Eastern Linn et al., 2002). The most common types ico Mountains form a 15-km-long, northwest- California shear zone appears to have been the of contractional structures are approximately trending range composed primarily of early dominant mode of postextensional deformation east-west–trending folds, many of which occur Miocene sedimentary and volcanic rocks in in the Mojave Desert region. Northwest-trending in Miocene lacustrine rocks. Folds are wide- the upper plate of the central Mojave metamor- right-lateral faults are ubiquitous and accom- spread across the region, suggesting that con- phic core complex (Fig. 1). Dacite and coarse modate a small percent of the relative motion traction is a regional phenomenon (Bartley et volcaniclastic sedimentary rocks of the Pick- between the Pacifi c and North American plates al., 1990). The magnitude of shortening repre- handle Formation compose most of the north- (Dokka and Travis, 1990b). East- to northeast- sented by these folds is not well documented, ern and central Calico Mountains (Fig. 1). The trending left-lateral faults are also common, par- and the timing of folding is unclear. Gently type locality of the Pickhandle Formation is in ticularly in the northeastern Mojave Desert. The folded Quaternary gravels indicate that some the northwestern Calico Mountains, where the cumulative amount of northwest-directed dex- folding is related to active strike-slip faults, and south- to southwest–dipping section is ~1500 m tral shear across the region is probably on the north-south shortening may play an important thick (McCulloh, 1952; Dibblee, 1994; Fig. 1). order of 50–75 km (Dokka and Travis, 1990a; role in present-day strain accumulation across Overlying the Pickhandle Formation are fi ne- Glazner et al., 2002). It is unclear when this the Eastern California shear zone (Oskin et al., grained lacustrine rocks generally considered faulting began, but some indirect evidence sug- 2007). The goal of this study is to understand part of the Barstow Formation and referred to in gests that northwest- trending dextral faults may the stratigraphic and structural evolution of the this study as the Calico Member of the Barstow have locally been active as early as 19 Ma (Bart- Calico Mountains, which arguably best exem- Formation. These lacustrine rocks are intruded 117o 00' Pc Explanation Mg lt 25 Barstow Fm. (ca. 17-13 Ma Garlock fau Tb lacustrine rocks) 50 Santa Barbara Tb Los Angeles San 45 Tp 45 Andr ca. 17 Ma dacitic intrusions 25 Tv eas 30 fault Mud Hills 25 45 Southern California Calico Member of Barstow Fm. Tbc (ca. 19-17 Ma lacustrine rocks 60 40 Tpv Pickhandle Fm. volcanic rocks Tbc? o 35 00' 40 35o 00' Pickhandle Fm. (early Miocene, 20 Tp Tp mostly coarse-grained Fort Irwin Rd. volcaniclastic rocks) 10 Mg TwgTTwwwgg Waterman Hills granodiorite 65 (early Miocene) Calico Mtns. Calico fa Mg Mesozoic plutonic rocks 65 ult 40 20 Metavolcanic rocks (Jurassic mv Sidewinder Fm.?) 35 40 Tbc ccm Tv Mylonitic rocks in the footwall 50 ccm of the central Mojave 45 40 45 metamorphic core complex Mitchel Range Study area mv Manix Paleozoic metasedimentary Hinkley Hills Lead Mtn. fault Pc and metavolcanic rocks 25 (Plate 1) Tp 70 = contact = bedding I-15 Yermo 25 attitude = anticline 30 mv = metamorphic Barstow n. 0 5 km = syncline foliation attitude and lineation trend = fault nt Mt ha = Waterman Hills o o detachment fault 117 00' 55 Elep 116 50' Figure 1.
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