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Provenance Evidence for Major Post–Early Pennsylvanian Dextral Slip on the Picuris-Pecos Fault, Northern New Mexico

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Provenance Evidence for Major Post–Early Pennsylvanian Dextral Slip on the Picuris-Pecos Fault, Northern New Mexico Provenance evidence for major post–early Pennsylvanian dextral slip on the Picuris-Pecos fault, northern New Mexico Steven M. Cather1, Adam S. Read1, Nelia W. Dunbar1, Barry S. Kues2, Karl Krainer3, Spencer G. Lucas4, and Shari A. Kelley1 1New Mexico Bureau of Geology and Mineral Resources, New Mexico Institute of Mining and Technology, Socorro, New Mexico 87801, USA 2Department of Earth and Planetary Sciences, University of New Mexico, Albuquerque, New Mexico 87131, USA 3Institute of Geology and Paleontology, University of Innsbruck, Innrain 52, Innsbruck A-6020, Austria 4New Mexico Museum of Natural History, 1801 Mountain Road NW, Albuquerque, New Mexico 87104, USA ABSTRACT INTRODUCTION Ancestral Rocky Mountain deformations, dex- tral slip on the Picuris-Pecos fault potentially The Picuris-Pecos fault is a major strike- The Proterozoic basement of the Southern contributed to crustal shortening in uplifts and slip fault in northern New Mexico (USA) Rocky Mountains in northern New Mexico, basins northwest of the fault (Fig. 1). that exhibits ~37 km of dextral separation of USA, has long been known to be dextrally The Picuris-Pecos fault formed the western Proterozoic lithotypes and structures. The faulted (Montgomery, 1963). Basement-related boundary of the late Paleozoic Taos trough dur- timing of dextral slip has been controversial aeromagnetic patterns have been interpreted to ing the early part of the Ancestral Rocky Moun- due largely to a lack of defi nitive piercing show net dextral offsets of ~55–130 km on sev- tain orogeny. During the Pennsylvanian, terranes points of Phanerozoic age. The Picuris- eral north-striking faults (Chapin, 1983; Cordell of distinctive Proterozoic lithotypes (metasedi- Pecos fault formed the western boundary of and Keller, 1984; Karlstrom and Daniel, 1993; mentary versus dominantly plutonic and meta- the late Paleozoic Taos trough. A distinctive Cather et al., 2006). The Picuris-Pecos fault is plutonic) were exposed in the upthrown western metasedimentary terrane that shed detritus the largest of these faults, with a dextral separa- block (the Uncompahgre uplift) of the Picuris- into the western Taos trough was exposed tion of ~37 km (Montgomery, 1963). Although Pecos fault. The paleolocations of these terranes on the Uncompahgre uplift west of the fault there is agreement that major dextral separa- can be ascertained using the provenance charac- during the early to middle Pennsylvanian. tions of Proterozoic rocks and structures exist teristics of Pennsylvanian strata in the adjoining We use the distribution of metasedimen- in northern New Mexico, the timing of dextral Taos trough, an approach that was pioneered by tary clasts and the age of monazite grains slip is controversial. This controversy derives in Sutherland (1963). We show that proximal Penn- within clasts from conglomeratic strata of part from the lack of defi nitive piercing points sylvanian (Morrowan? to early Desmoinesian) the western Taos trough to determine the in Phanerozoic rocks of the region. As a result, petrofacies are today mismatched from their paleolocation of the southern boundary of dextral slip has variously been inferred to have distinctive source terranes west of the fault. We this metasedimentary terrane during the occurred primarily during the Proterozoic utilize clast composition and monazite geochro- middle Pennsylvanian (Desmoinesian), and (Montgomery, 1963; Yin and Ingersoll, 1997; nology as provenance indicators to show that thereby quantify the subsequent separa- Fankhauser and Erslev, 2004; Wawrzyniec et al., ~40–50 km of dextral slip has occurred on the tion on the fault. The rematching of detri- 2007), mostly during the late Paleozoic Ances- Picuris-Pecos fault since the early Pennsylvanian. tal petrofacies with source terranes in the tral Rocky Mountain orogeny (Baars and Ste- adjacent uplift requires ~40–50 km of dex- venson, 1984; Woodward et al., 1999), mostly BACKGROUND tral separation on the Picuris-Pecos fault during the Late Cretaceous–Eocene Laramide since the early Desmoinesian. This exceeds orogeny (Chapin and Cather, 1981; Chapin, The Picuris-Pecos fault is the best exposed the present ~37 km dextral separation of 1983; Karlstrom and Daniel, 1993; Daniel et al., and most studied of the dextral faults in north- Proterozoic features by the fault, and thus 1995; Bauer and Ralser, 1995; Cather, 1999), or ern New Mexico (Fig. 2). The fault strikes north, implies that an ~3–13 km sinistral separa- during both the Ancestral Rocky Mountain and dips steeply west, and cuts rocks ranging in age tion existed on the fault in the early Des- Laramide orogenies (Cather, 2004; Cather et from Proterozoic to Paleogene. It is exposed moinesian. The ~40–50 km of post–early al., 2006). The possible regional kinematic role for ~80 km along strike, and may extend the Desmoinesian dextral separation on the of the Picuris-Pecos fault during Proterozoic length of the state (~600 km) if probable fault Picuris-Pecos fault is the result of slip that deformations is unclear; regional strain analysis linkages to the north and south are considered accumulated late in the Ancestral Rocky suggests lateral slip on the fault during known (Cather and Harrison, 2002; Cather, 2009). With Mountain deformation and/or during the Proterozoic deformations was probably sinistral ~37 km dextral separation of Proterozoic litho- Laramide orogeny. (Cather et al., 2006). During the Laramide and types and east-west–trending ductile structures, Geosphere; October 2011; v. 7; no. 5; p. 1175–1193; doi: 10.1130/GES00649.1; 22 fi gures; 1 table; 1 supplemental fi le. For permission to copy, contact [email protected] 1175 © 2011 Geological Society of America Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/7/5/1175/3340900/1175.pdf by guest on 25 September 2021 Cather et al. the Picuris-Pecos fault exhibits the largest mud that fi lls fi ssures and the interstices of brec- of the fault shared similar ca. 1.2–0.4 Ga cool- known separation of any fault in the central and cias in the damage zone of the fault (Erslev et al., ing histories and passed into the purely brittle Southern Rocky Mountains. It exceeds that of 2004; Fankhauser, 2005; Cather et al., 2008). Slip regime (<300–250 °C) during or soon after the the next largest fault (the Wind River thrust) by on the Picuris-Pecos fault during both the Ances- Grenville orogeny (ca. 1.2–0.9 Ga; Sanders et a factor of nearly two. tral Rocky Mountain and Laramide orogenies al., 2006). Modest west-up components of slip The Picuris-Pecos fault has been repeatedly had a west-up component (Sutherland, 1963), but on the Picuris-Pecos fault defi ned the western reactivated. During the Proterozoic, plutonism, regional strain balancing suggests that it also may margin of the Ancestral Rocky Mountain Taos ductile deformation, and peak metamorphism have hosted signifi cant dextral slip during these trough (Casey, 1980) during the early Penn- in northern New Mexico occurred ca. 1.4 Ga deformations (Cather et al., 2006). sylvanian, but topographic relief on this basin (Williams et al., 1999a). The lack of mylonites Several lines of evidence indicate that the margin was low enough that it was lapped over along the Picuris-Pecos fault, however, suggests Picuris-Pecos fault did not accommodate major and buried by marine strata during the middle that no ductile precursor to the fault was active at dip slip. Metasedimentary rocks exposed in the Pennsylvanian (early to middle Desmoines- the time (Cather et al., 2006). Subsequent brittle Picuris and Truchas Mountains are separated ian; see following). West-up components of slip along the Picuris-Pecos fault, however, may by the Picuris-Pecos fault, but show evidence slip also occurred on the Picuris-Pecos fault have occurred during the Grenville orogeny and for similar peak metamorphic conditions near during Laramide deformation, but similar late during Neoproterozoic deformation related to the the Al-silicate triple point (3.5–4.0 kbar, 500– Laramide apatite fi ssion-track cooling ages breakup of Rodinia (Cather et al., 2006). The ear- 550 °C; Grambling, 1979, 1981; Daniel et al., occur at similar elevations on both sides of the liest undisputable evidence for slip on the fault 1995). Thermochronologic data from the south- fault (Kelley and Chapin, 1995, their fi g. 8) and is early in the Ancestral Rocky Mountain orog- ern Sangre de Cristo Mountains indicate that suggest that Laramide differential uplift across eny, as shown by Mississippian marine carbonate rocks at similar modern elevations on both sides the fault was not large. The observed ~37 km of dextral separation on the Picuris-Pecos fault must therefore be largely the result of strike slip. STUDY AREA The study area encompasses the central part of the Picuris-Pecos fault adjacent to the Tru- chas uplift (Fig. 3). Outcrops north of the Tru- chas uplift are near roads, but areas to the south are within the Pecos Wilderness and are acces- sible only by foot or on horseback. Within the study area no major faults intersect the Picuris- Pecos fault, resulting in a relatively simple structural geometry. The Picuris-Pecos fault transects and offsets two distinctive terranes of Proterozoic rocks. The southern terrane consists of ca. 1.72–1.44 Ga metaplutonic, plutonic, and subordinate metavolcanic rocks, granitic gneiss and granite being the volumetrically dominant lithotypes (Karlstrom et al., 2004). The northern terrane is dominated by metasedimentary rocks (Hondo Group, ca. 1.69 Ga) and subordinate metavolcanic rocks (Vadito Group, ca. 1.70 Ga). Metasedimentary rocks of the Hondo Group include the Ortega Quartzite and schist, phyllite, and quartzite of the Rinconada, Pilar, and Piedra Lumbre Formations. The Proterozoic terranes are separated by a 200 major south-dipping ductile thrust fault. East of the Picuris-Pecos fault this fault is termed the Pecos thrust; to the west it is termed the Plomo fault (Fig.
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