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Paleomagnetic Data Bearing on Vertical Axis Rotation of the Rio Del Oso Dike Swarm, Western Española Basin, New Mexico

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Paleomagnetic Data Bearing on Vertical Axis Rotation of the Rio Del Oso Dike Swarm, Western Española Basin, New Mexico Paleomagnetic data bearing on vertical axis rotation of the Rio del Oso dike swarm, western Española Basin, New Mexico Petronis, M.S.1, Trujillo, R.V.1, 2, Lindline, J.1, and Zebrowski, J.P.1 1Environmental Geology, Natural Resources Management Department, New Mexico Highlands University, P.O. Box 9000, Las Vegas, NM 87701 2New Mexico Environment Department, Air Quality Bureau, 525 Camino de los Marquez, Suite 1, Santa Fe, New Mexico, 87505-1816 Abstract 1994). The rift extends south from crustal blocks. To assess this hypothesis, about Leadville, Colorado and merges we obtained paleomagnetic data from The Española Basin is one of a series of interconnected, asymmetrical basins in the with the eastern Basin and Range Miocene mafic intrusions of the Rio del Rio Grande rift that includes a number of Province of eastern Arizona, New Oso dike swarm (Koning et al., 2007) north- and northeast-striking faults that accom- Mexico, and northern Mexico (Fig. 1). in the western Española Basin. We also modated block tilting and basin subsidence. Characteristics of the rift include high conducted petrographic examination of The western margin of the Española Basin, in heat flow, structurally-controlled basins, the studied intrusions to confirm their particular, is characterized by a greater than 17-km wide zone of normal and oblique-slip crustal deformation, and Cenozoic to affinity to the regionally extensive extru- faults. To clarify the involvement of block rota- Holocene silicic to mafic volcanism. The sive basalts of the Lobato Formation. tion in the tectonic evolution of the Española high heat flow is attributed to upper Basin, we carried out a paleomagnetic study mantle asthenospheric upwelling and of mafic intrusions (Rio del Oso dike swarm) thermal lithospheric erosion (Seager Geologic and tectonic that are genetically related to regionally exten- sive basalt flows of the mid-Miocene Lobato and Morgan, 1979; Morgan et al., history of the Formation. The primary hypothesis tested 1986; Wilson et al., 2005). In northern Española Basin was that these intrusions experienced some New Mexico and southern Colorado, degree of vertical axis rotation associated with the structural manifestation of the rift mid-Miocene to recent continental rifting. In is a series of right-stepping, asymmetric The Española Basin, located in situ paleomagnetic results from forty-two sites yield a group mean declination (D) of 344.0°, fault-bounded en echelon basins with north-central New Mexico, is bordered extension increasing southward (Kelley, by the Nacimiento uplift to the west and an inclination (I) of 41.1°, α95 of 6.1°, and k of 14.1. The group mean result is discordant 1982). From north to south, these are the Sangre de Cristo Mountains to the to the <10 Ma pole of D=356.0°, I=54.4°, α95 the upper Arkansas River Basin, San east (Fig. 1). The Española Basin likely = 3.3° with a statistically significant inferred Luis Basin, Española Basin, Albuquer- developed by about 26 Ma and was rotation (R) of -12.0°± 7.2° and flattening of +13.3° ± 5.5° relative to the <10 Ma pole field que Basin, and the southern Rio Grande initially ~3 km deep during the Oligo- direction. These discordant results indicate that Basin (Fig. 1). Rift deformation from ca. cene (Golombek et al., 1983). Renewed a modest degree of counter-clockwise vertical 30 to 20 Ma resulted in a broad zone tectonism during the early Miocene axis rotation occurred in this region, which is of distributed extension along low-angle resulted in localized faulting that led to likely associated with Rio Grande rifting north faults, crustal doming, widespread significant accumulations of sediment in of the Jemez Mountains. It is possible that oblique motion along the Santa Clara fault and/ magmatic activity, and accumulation of the north and central parts of the basin or the Cañada del Almagre fault facilitated the sediment in intrarift basins (Chapin, with thicknesses reaching up to 5 km vertical axis rotation. The results from this study 1988; Prodehl and Lipman, 1989). (Aldrich, 1986; Golombek et al., 1983). imply that vertical axis rotation is common to Between ca. 20 and 10 Ma, the rate The rift-basin deposits are collectively extensional rift systems and should be considered of extension accelerated with rifting referred to as the Santa Fe Group. At when modeling continental extension. restricted to a narrower zone and approximately 10 Ma, basin subsid- characterized by high-angle normal ence slowed and sediment aggradation faulting and the onset of alkalic mafic ensued, resulting in thick deposits of Introduction magmatism (Golombek et al., 1983; the Santa Fe Group within the Española Prodehl and Lipman, 1989; Baldridge Basin (Aldrich and Dethier, 1990). In The Rio Grande rift is a roughly et al., 1991). The rate of extension has addition, between 15 Ma and 14 Ma, north-south trending intracratonic rift decreased in the last 5 Ma, but the rift volcanism occurred at the northwestern that separates the over thickened and remains seismically and magmatically edge of the basin (Aldrich and Dethier, relatively undeformed continental crust active (Grauch et al., 2017). We hypoth- 1990) along the Jemez Lineament, a of the Colorado Plateau on the west esize that Rio Grande rift faulting in complex suture zone between the Meso- from the stable craton of the Great the northwestern Española Basin was proterozoic Yavapai and the Mazatzal Plains to the east (Kelley, 1977; Aldrich accommodated by extension and count- lithospheric provinces that facilitated and Dethier, 1990; Chapin and Cather, er-clockwise rotation of fault-bounded volcanism and tectonism near the Jemez Fall 2020, Volume 42, Number 2 61 New Mexico Geology 107°W 106°30'W 106°W 105°30'W Taos EF 36°N 36°N Los Alamos PFZ P-PF Santa Fe LBF 35°30'N 35°30'N SFF Bernalillo T-CF Albuquerque 35°N SF 35°N 106°30'W 106°W 105°30'W Faults 50 Tertiary-Quaternary Volcanics Kilometers Tertiary Intrusions Tertiary Espinaso Formation Figure 1. Inset: General sketch map depicting the Rio Grande rift and related sub-basins throughout southern Colorado, New Mexico, and Mexico (modified from Grauch and Bankey, 2003). Tectonic map of part of northern New Mexico showing the location of the the Española block. T-CF—Tijeras-Cañoncito fault zone; PFZ—Pajarito fault zone; EF—Embudo fault zone; P-PF—Picuris-Pecos fault zone; LBF—La Bajada fault; SFF—San Felipe fault; SF—Sandia fault. Red rectangle indicates area shown in the Figure 2 map. Location map modified from http://cires.colorado.edu/science/groups/sheehan/projects/riogrande/ images/faq2.jpg. Faults on tectonic map are from the U.S. Geological Survey Quaternary fault and fold database (http://gldims.cr.usgs.gov); geologic units are from NMBGMR (2003). Fall 2020, Volume 42, Number 2 62 New Mexico Geology Mountains and locally throughout the (the Rio del Oso dike swarm) located are often argued to be interconnected Rio Grande rift (Aldrich, 1986; Wolff et in the Chili 7.5’ quadrangle (Koning et at depth (e.g., Baer, 1991). Anderson al., 2005). Jemez Mountain volcanism al., 2005). Intrusions associated with (1951) proposed that dike segmen- began with the eruption of the Lobato Lobato Formation basalts contain 1 to tation may be attributed to rotation Formation basalts from numerous 2 mm crystals of plagioclase, olivine, of the minimum principle stress (σ3) vents until approximately 10 Ma. At and augite. toward the surface during magma ~9 Ma, volcanism slowed drastically intrusion. We sampled at least eight with only minor Lobato volcanism Geology of the Chili distinct intrusions at four locations continuing until ~7 Ma (Aldrich and spread over an ~4.8 km2 area, although Dethier, 1990). The end of basaltic quadrangle the number of sampled intrusions is a volcanism in this area is thought to be minimum estimate because of difficulty related to a change in the regional stress Dikes in the Rio del Oso swarm were tracing individual dikes along strike. field. This switch is evident throughout studied in the northwest corner of the The dikes intrude Miocene Santa Fe western North America and has been Chili quadrangle, which lies north of Group deposits and form prominent inferred to reflect reorganization of the intersection of the Jemez Lineament ridges across the landscape (Fig. 3). North American-Pacific plate bound- and the western margin of the Española The dikes have been dated by the ary conditions (Golombek et al., 1983; Basin in Oso Arroyo just west of K-Ar method to yield age estimates Prodehl and Lipman, 1989; Atwater Chili, New Mexico (Fig. 1). The Chili of 9.7 ± 0.3 Ma, 10.7 ± 0.3 Ma, and and Stock, 1998). quadrangle is situated in a structurally 10.6 ± 0.3 Ma (Baldridge et al., 1980). diverse part of the basin that exhibits Likely correlative lava flows from the a complex brittle kinematic history area have a similar mineralogy as the Lobato Formation Basalts (Koning et al., 2005; Fig. 1). A variety intrusions and yield age determinations of rift-related geologic features as old that range from 9.6 ± 0.2 Ma to 12.4 The Lobato Formation basalts are the as middle Miocene are well-exposed Ma (Dethier et al., 1986, Dethier and oldest unit of the Polvadera Group, in the area. These features include an Manley, 1985). which crops out on the northern to array of normal and strike-slip faults, No detailed paleomagnetic studies eastern flanks of the Jemez Mountains a relatively complete sequence of have been conducted on the dikes in and forms prominent mesas through- middle to upper Miocene and Pliocene this area. In northern New Mexico, out the area (Smith, 1938; Koning rift-basin sediments, upper Miocene several paleomagnetic studies (Brown et al., 2005).
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