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Great Valley Nevada Sierra Peninsular Ranges

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Great Valley Nevada Sierra Peninsular Ranges Jacobson et al. PSP 121°W Faults Pelona-Orocopia-Rand Schists Forearc sampling areas Ef Elsinore BR Blue Ridge AT Atascadero Diablo DP EHf East Huasna CD Castle Dome Mountains BL Ben Lomond Mountain Great Gf Garlock CH SE Chocolate Mountains CA Cambria PP BL Nf Nacimiento EF East Fork CL Coalinga 37°N Rf Rinconada MP Mount Pinos CP Cajon Pass SAf San Andreas NR Neversweat Ridge DP Del Puerto Canyon Range SGf San Gabriel OR Orocopia Mountains IR Indians Ranch SGHf San Gregorio-Hosgri PR Portal Ridge LP La Panza Range PL SS SJf San Jacinto RA Rand Mountains NB Northern Baja California SL PS SYf Santa Ynez SC Santa Catalina Island OR Orocopia Mountains CL SE San Emigdio Mountains PL Point Lobos IR Sierra 36°N Valley SP Sierra Pelona PM Pine Mountain Block Rf Nf SS Sierra de Salinas PP Pigeon Point TR Trigo Mountains PS Point Sur Nevada PSP Point San Pedro CA AT SA Northern Santa Ana Mts. SGHf LP RA SC Santa Catalina Island SAf SD San Diego Gf SG San Gabriel block 35°N Salinian block EHf SAf SMM SGHf Nf SE SL NW Santa Lucia Range MP SM Santa Monica Mts-Simi Hills SR Nacimiento blk PM SG PR SMI San Miguel Island SYf SR SMM Sierra Madre Mountains Nf BR SY SY SP SG CP SR San Rafael Mountains CTR WTR EF SY Santa Ynez Mountains SMI SM 34°N SGf ETR McCoy Mts. Fm. WTR SA Peninsular OR Accretionary complex SC N SJ Forearc basin f SAf TR CD Ranges NR Magmatic arc and wall rocks Ef CH CA Pelona-Orocopia-Rand Schists 100 km SD MEX AZ McCoy Mountains Formation 118°WNB 115°W Jacobson et al., GSA Bull, 2010 Figure 1. Generalized late Mesozoic–early Cenozoic geology of central to southern California and adjoining areas, based largely on Jennings (1977). Some outcrops of arc rocks and older wall rocks were omitted from southeasternmost California and southwesternmost Arizona to emphasize outcrops of Pelona-Orocopia-Rand schist and McCoy Mountains Formation. Inset delineates the Salinian and Nacimiento blocks. The Nacimiento fault is indicated by a heavier line weight than the other faults. We follow the interpretation of Hall et al. (1995) and Dickinson et al. (2005) that the Nacimiento fault has been offset ~45 km in a dextral sense by slip on the combined Rinconada–East Huasna fault. Sample localities for both Pelona-Orocopia-Rand schists and forearc units are indicated. Repeated labels (SG, SY, and SR) indicate the grouping of samples collected over relatively large areas. Abbreviations not defi ned in the fi gure: AZ—Arizona; CA—California; CTR—central Transverse Ranges; ETR—eastern Transverse Ranges; MEX—Mexico; WTR—western Transverse Ranges. involved remain unclear. Previous interpreta- 1978; Ehlig, 1981; Jacobson et al., 1988). These Orocopia-Rand schists has long been debated tions include thrusting of 150–200 km (Silver, rocks broadly resemble the Franciscan Com- (Haxel et al., 2002; Grove et al., 2003), although 1983; Hall, 1991; Barth and Schneiderman, plex, but instead of being positioned outboard most workers now favor a model involving low- 1996; Saleeby, 1997; Ducea et al., 2009), dex- of the forearc basin, they sit in structural contact angle subduction of the Farallon plate during the tral strike slip of 2000 km or more (Page, 1982; directly beneath the Cretaceous marginal batho- Laramide orogeny (Crowell, 1968, 1981; Yeats, Champion et al., 1984), and sinistral strike slip lith and adjoining cratonal areas of southeastern 1968; Burchfi el and Davis, 1981; Dickinson, of 500–600 km (Dickinson, 1983; Seiders and California and southwestern Ari zona. Poten- 1981; Hamilton, 1988; May, 1989; Malin et al., Blome, 1988; Dickinson et al., 2005). tially equivalent rocks, recovered as xenoliths, 1995; Jacobson et al., 1996, 2002, 2007; Wood A second key feature of southern and coastal occur still farther east in the Four Corners region and Saleeby, 1997; Yin, 2002; Grove et al., central California is represented by the Pelona- of Arizona, New Mexico, Utah, and Colorado 2003; Saleeby, 2003; Kidder and Ducea, 2006; Orocopia-Rand schists (Fig. 1; Haxel and Dillon , (Usui et al., 2006). The origin of the Pelona- Saleeby et al., 2007). 486 Geological Society of America Bulletin, March/April 2011 Exhumation of the Orocopia Schist and associated rocks of southeastern California 5 Figure 3. Geology of the Orocopia Mountains and vicinity (after Crowell, 1975). Contacts within the northwestern half of the upper plate of the Orocopia Mountains detachment fault were modifi ed based on this study. Those in the southeastern half were modifi ed based on the work of Ebert (2004). Lines A–A′ to C–C′ indicate locations of cross sections illustrated in Figure 4. PC—Painted Canyon. Jacobson et al., GSA SP 419, 2007 3. The Orocopia Mountains detachment fault is folded by the schist and upper plate (Orocopia Mountains detachment fault) A reminder of typical geology. Schists are meta-turbiditesthe Chocolate Mountainswith some anticlinorium. metabasite, Consequently, chert and serpentinite. dating the andInverse placed mmic a greater gradients emphasis often on found relating but thermomodern chronologic exposure is typically under extensional fault systems. “The Pelona-Orocopia-Rand schists consist of 90% or more quartzo-feldspathic schist presumably derived from turbidite sandstone (Ehlig, 1958, 1981; Haxel and Dillon, 1978; Jacobson et al., 1988, 1996; Haxel et al., 1987, 2002). The schists also include up to 10% metabasite, along with minor amounts of Fe-Mn meta- chert, marble, serpentinite, and talc-actinolite rock. Metamorphism occurred under conditions of moderately high pressure relative to tem- perature. Mineral assemblages lie mostly within the greenschist and albite-epidote amphibolite faciesfault but locally provides extend into the epidote-blue-a maximum schist and ageupper amphibolite for the facies anticlinorium, (Ehlig, 1981; Haxel and Dillon,which 1978; hasGraham andresults Powell, 1984; to Jacobson fabric and Sorensen, elements 1986; Jacobson within et al., 1988; the Kidder schist. and Ducea, In 2006). contrast, Inverted metamorphic Ebert zonations are typical. Initial em- placement of the schists is attributed to a Late Cretaceous–early Cenozoic low- angle fault sys- tem referred to as the Vincent–Chocolate Moun- tains thrust (Haxel and Dillon, 1978). However, most present-day contacts between the schists and North American upper plate appear to be low-angle normal faults related to exhumation of the schists, either shortly after underthrust- ing or during middle Cenozoic extension (Frost et al., 1982; Hamilton, 1988; Jacobson et al., 1988, 2002, 2007; Malin et al., 1995; Wood and Saleeby, 1997; Haxel et al., 2002).”-Jacobson et al., 2010 implications for the passive-roof thrust model of Yin (2002). et al. (2003), Ebert (2004), and Ebert and Yin (2004) focused To investigate the above issues, we performed 40Ar/39Ar on detailed mapping within the upper plate and analysis of the step-heating experiments with hornblende, muscovite, biotite, C l e m e n s W e l l f a u l t . and K-feldspar to constrain the temperature-time histories for Whereas the vast majority of the new data obtained in this both the schist and upper plate in the Orocopia Mountains. study come from the Orocopia Mountains, we also report 40Ar/39Ar Additional control is provided by several apatite fi ssion track step-heating results for three new samples of K-feldspar from the ages, ion microprobe U-Pb dating of zircon from a Late Creta- Orocopia Schist of the Gavilan Hills. These new data were col- ceous leucogranite within the upper plate, and previous U-Pb lected to facilitate comparisons of thermal history between the dating of detrital zircon from the schist (Jacobson et al., 2000; two regions. Grove et al., 2003). The thermochronologic results were inte- grated with preexisting and new observations on the structural REGIONAL BACKGROUND and metamorphic evolution of the schist and upper plate. As detailed below, these data reveal a two-stage exhumation his- The Orocopia Schist of the Orocopia Mountains is exposed tory for the schist in the Orocopia Mountains very much like in a northwest-trending, postmetamorphic antiform that defi nes that found in the Gavilan Hills. the northernmost culmination of the Chocolate Mountains anti- The present study concentrated on the western to northwest- clinorium (Figs. 3 and 4). Proterozoic to Cretaceous igneous and ern part of the Orocopia Mountains (Fig. 3). A similar investiga- metamorphic rocks of the upper plate crop out in a narrow belt tion has recently been conducted by Ebert et al. (2003), Ebert that sits above the schist along the Orocopia Mountains detach- (2004), and Ebert and Yin (2004) in the southeastern part of the ment fault. The structure, metamorphism, and thermochronology range. Our work focused more heavily on the contact between of the schist and upper plate are described in detail below. Downloaded from specialpapers.gsapubs.org on March 8, 2010 384 M. Grove et al. depositional age for the graywacke protolith for all of the schists and reveal systematic regional variations in the depositional age and provenance of the protolith. When combined with 40Ar/39Ar cooling ages, our detrital zircon U-Pb data can be used to constrain the “cycling interval” during which the schist’s graywacke protolith was eroded from its source region, deposited, underthrust, accreted, and metamor- phosed beneath crystalline rocks of southwestern North America. Combined with previously obtained data, new muscovite and biotite 40Ar/39Ar cooling ages from our detrital zircon samples clearly indicate that the cycling interval for erosion, deposition, underthrusting, accretion, and metamorphism varied systemati- cally across the schist terrane. Schist located outboard of the cra- ton in the southern Coast Ranges and northwestern Mojave Des- ert was emplaced well before schists were underplated beneath more cratonal (and progressively more southeasterly) positions in the Transverse Ranges and southeastern California and south- western Arizona.
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