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Stratigraphic Record of Pleistocene Faulting and Basin Evolution in the Borrego Badlands, San Jacinto Fault Zone, Southern California

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Stratigraphic Record of Pleistocene Faulting and Basin Evolution in the Borrego Badlands, San Jacinto Fault Zone, Southern California Stratigraphic record of Pleistocene faulting and basin evolution in the Borrego Badlands, San Jacinto fault zone, Southern California Andrew T. Lutz Rebecca J. Dorsey† Department of Geological Sciences, 1272 University of Oregon, Eugene, Oregon 97403-1272, USA Bernard A. Housen Department of Geology, Western Washington University, Bellingham, Washington 98225-9080, USA Susanne U. Janecke Department of Geology, Utah State University, Logan, Utah 84322-4505, USA ABSTRACT the western Borrego Badlands postdates a useful tool for documenting changes in the Ocotillo deposition, and thus appears to have position and behavior of basin-bounding faults Sedimentary rocks in the Borrego Bad- propagated southeast into the study area at through time, because it records dynamic inter- lands, Southern California, contain a record ca. 0.6 Ma. actions between subsidence and sediment input of Pleistocene crustal deformation during The Fonts Point Sandstone is a thin, sheet- that are commonly controlled by faulting in tec- initiation and evolution of the San Jacinto like alluvial deposit that records the end of tonically active regions (e.g., Paola et al., 1992; fault zone. We used detailed geologic, strati- deposition and onset of transpressive defor- Gawthorpe et al., 1994, 1997; Paola, 2000). Thus graphic, and paleomagnetic analysis to deter- mation in the Borrego Badlands. The base we can use our knowledge of tectonic controls mine the age and geometry of the deposits and of the Fonts Point Sandstone changes from a on stratigraphic evolution to better understand reconstruct the history of fault-controlled conformable contact in a narrow belt south- the late Cenozoic evolution of the San Andreas sedimentation in this area. The base of the east of the Inspiration Point fault, where it is fault system in the western Salton Trough. ~300 to 500 m thick Ocotillo Formation is a dated at 0.6 ± 0.02 Ma, to an angular uncon- The western Salton Trough contains over paraconformity to abrupt conformable con- formity on the folded Ocotillo Formation 6 km of upper Miocene to Pleistocene sedimen- tact that records a brief hiatus followed by northwest of the fault. The pattern of stratal tary rocks that record crustal deformation and rapid progradation of coarse alluvial sedi- truncation records initiation of the Inspira- basin subsidence during evolution of the San ment over lacustrine facies of the Borrego tion Point fault at ca. 0.6 Ma. This coincides Andreas plate-boundary system in Southern Formation at 1.05 ± 0.03 Ma. This coincides with a major structural reorganization in the California (Dibblee, 1954, 1984, 1996; Wood- with regional-scale progradation of Ocotillo San Jacinto fault zone that initiated the mod- ard, 1963, 1974; Kerr, 1982; Winker, 1987; Formation sand and gravel, and appears to ern phase of north-south shortening and ero- Kerr and Kidwell, 1991; Winker and Kidwell, record initiation of strike-slip faults in the sion in the southwestern Salton Trough. 1996). Recent studies have shown that, from late southwestern Salton Trough at ca. 1.1 Ma. Miocene to early Pleistocene time, formation of Thickness trends, clast compositions, paleo- Keywords: stratigraphy, San Jacinto fault, this basin was controlled by combined slip on currents, and distribution of paleosols pro- Pleistocene, California, basin analysis. the San Andreas fault in the northeast and the vide evidence for initiation of the East Coy- West Salton detachment fault in the west (Axen ote Mountain fault at ca. 1.05 Ma, followed INTRODUCTION and Fletcher, 1998; Dorsey, 2006; Steely, 2006; by onset of NNE-ward basin tilting obliquely Kirby et al., in press). The change from regional toward the Santa Rosa segment of the Clark The San Andreas fault system in Southern transtension and detachment faulting to strike- fault at ca. 1.0 Ma. Stratigraphic omission California is a complicated zone of active strike- slip faulting and transpression resulted from a of the Ocotillo Formation and progressively slip faults and related crustal deformation that major tectonic reorganization in late Pliocene or older units southwest of the Coyote Creek accommodates ~50 mm/yr of relative motion early Pleistocene time, but the timing and style fault beneath the Fonts Point Sandstone between the Pacifi c and North American plates of this transition are poorly understood. As a provides evidence that tilting to the north- (Fig. 1) (DeMets et al., 1990; Bennett et al., result, our understanding of Pliocene-Pleisto- northeast was related in part to growth of the 1996; DeMets and Dixon, 1999; McCaffrey, cene regional kinematics and plate-boundary San Felipe anticline during deposition of the 2005; Meade and Hager, 2005). While the loca- deformation in Southern California is limited. Ocotillo Formation. Map and stratigraphic tion and seismic expression of faults in this zone This paper documents the stratigraphy and data suggest that the Coyote Creek fault in are relatively well known, the partitioning of architecture of the Pleistocene Ocotillo Forma- strain in space and time, and the long-term evo- tion and Fonts Point Sandstone in the Borrego †Corresponding author e-mail: rdorsey@uoregon. lution of faults at geologic time scales (106 yr), Badlands, near the western margin of the Salton edu. remain poorly understood. Stratigraphy provides Trough (Fig. 1). A thick sequence of alluvial, GSA Bulletin; November/December 2006; v. 118; no. 11/12; p. 1377–1397; doi: 10.1130/B25946.1; 15 fi gures; 1 table, Data Repository item 2006217. For permission to copy, contact [email protected] 1377 © 2006 Geological Society of America Lutz et al. 117oW 115oW the hanging wall of the West Salton detachment r Santa Rosa Mtns SAF SAF fault system (e.g., Axen and Fletcher, 1998; WSDF ive Dorsey, 2006). This large basin was segmented N do R o SJFZ S 34 30'N AF into two separate subbasins by initiation of the o Colora intervening dextral-normal San Felipe fault EF A Fig.1b zone, perhaps as recently as ca. 1.1 Ma (Kirby, Pacific Ocean Salton 2005; Kirby et al., in press; Steely et al., 2005; SD IF CF SRF USA Steely, 2006). Mexico Sea Upper Miocene to Pleistocene sedimentary CCF N o San Ysidro km N rocks in the western Salton Trough record ini- 32 Mtns A 0 50 BB SFH tiation, evolution, and deactivation of the West BRAWLEY SEISMIC ZONE Salton detachment fault system (Fig. 2). Older SFF SFA deposits overlie crystalline basement that YR Quaternary Fig. 3 Rhyolite includes Cretaceous tonalite and granodiorite, pre-Cretaceous metasedimentary rocks, and OB a fault Vallecito CCF EVF Extr Late Cretaceous mylonite formed by regional Mtns EF ERF top-to-the-west thrusting (Sharp, 1967; Dib- blee, 1954; Jahns, 1954; Gastil, 1975; Engel and N 33 WSDF o Fish SHF Schultejann, 1984; Calzia et al., 1988; Simpson, 33 FCVB Creek 1984). Upper Miocene, rift-related nonmarine Mtns SMF Mesquite deposits of the Split Mountain Group are locally Tierra Basin Blanca preserved and are overlain by widespread marine Mtns strata of the lower Pliocene Imperial Formation (Woodard, 1963; Dibblee, 1954; Kerr, 1982; EF 0 10 20 30 km IF B N Winker, 1987; Kerr and Kidwell, 1991; Winker and Kidwell, 1996; Dorsey et al., in press). o 116o W 115o 30' W 116 30' W The Pliocene Palm Spring Formation was Quaternary Late Cenozioc Paleozoic metsedimentary and originally described by Woodard (1963) and alluvium sedimentary rocks Mesozoic plutonic rock was later redefi ned as a group that includes the Figure 1. (A) Fault map of Southern California, modifi ed from Sharp (1967). (B) Generalized Diablo and Olla Formations, Canebrake Con- geologic map of the western Salton Trough. A—Anza; BB—Borrego Badlands; CCF—Coyote glomerate, and Borrego Formation (Winker and Creek fault; CF—Clark fault; EF—Elsinore fault; ERF—Elmore Ranch fault; EVH—Earth- Kidwell, 1996). The Diablo Formation is 1– quake Valley fault; FCVB—Fish Creek–Vallecito basin; IF—Imperial fault; OB—Ocotillo 2 km thick and contains Colorado River–derived Badlands; SAF—San Andreas fault; SD—San Diego; SFA—San Felipe anticline; SFF—San fl uvial-deltaic sandstone and mudstone that pass Felipe fault; SFH—San Felipe Hills; SHF—Superstition Hills fault; SJFZ—San Jacinto fault laterally into coarse basin-margin facies of the zone; SMF—Superstition Mountain fault; SRF—Santa Rosa fault; WSDF—West Salton Olla Formation and Canebrake Conglomerate detachment fault; YR—Yaqui Ridge. Adapted from a map originally compiled by L. Seeber, (Dibblee, 1954; Morley, 1963; Hoover, 1965; modifi ed after Axen and Fletcher (1998), Steely (2006), Kirby et al. (in press), Kirby (2005). Reitz, 1977; Winker, 1987; Winker and Kidwell, 1996). Sandstone units represent deposits of a meandering channel system, and siltstone and claystone are interpreted as overbank facies, fl uvial, and lacustrine sediments in this area GEOLOGIC BACKGROUND similar to deposits of the modern Colorado records crustal tilting and sedimentation that River delta system in the Salton Trough (Dib- took place between the modern traces of the Regional Stratigraphy blee, 1954; Winker, 1987). Clark and Coyote Creek faults. Detailed study The Borrego Formation is a thick, region- of these deposits provides new information The western Salton Trough is a structurally ally extensive unit of lacustrine claystone, about the timing and style of faulting that con- complex region of fault-bounded basement mudstone, and marlstone with minor sandstone trolled Pleistocene sedimentation in the Borrego uplifts and fl anking sedimentary basins (Fig. 1) and siltstone that overlies and is in part later- Badlands. Comparison with companion studies that formed in response to late Cenozoic rift- ally equivalent to the Diablo Formation (Fig. 2) in the San Felipe Hills (Kirby, 2005; Kirby et ing and transtensional strain adjacent to the San (Tarbet and Holman, 1944; Dibblee, 1954, al., in press) and northern Vallecito Mountains Andreas fault (e.g., Dibblee, 1954; Woodard, 1984; Morley, 1963; Bartholomew, 1968; Dro- (Steely et al., 2005; Steely, 2006) suggests that 1963; Winker, 1987; Winker and Kidwell, nyk, 1977; Reitz, 1977; Wagoner, 1977; Ferra- widespread progradation of the Ocotillo Forma- 1996).
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