Castle Valley and ABSTRACT Known Basement Ages in the Nearby Uncompahgre Uplift

Home , Cutler Formation, Eolianite, Fisher Towers, Kaibab Limestone, Organ Rock Formation, Paradox Formation

Research Paper

GEOSPHERE Provenance of a Permian erg on the western margin of Pangea: Depositional system of the Kungurian (late Leonardian) Castle GEOSPHERE; v. 11, no. 5, p. 1475–1506 Valley and White Rim sandstones and subjacent Cutler Group, doi:10.1130/GES01174.1

14 figures; 3 tables; 1 supplemental file Paradox Basin, Utah, USA Timothy F. Lawton1, Cody D. Buller2, and Todd R. Parr3 CORRESPONDENCE: tlawton@geociencias 1Centro de Geociencias, Universidad Nacional Autónoma de México, Querétaro, 76230, México .unam.mx 2RKI Exploration & Production, 210 Park Avenue #700, Oklahoma City, Oklahoma 73102, USA 3Apache Corporation, 2000 Post Oak Boulevard, Houston, Texas 77056, USA CITATION: Lawton, T.F., Buller, C.D., and Parr, T.R., 2015, Provenance of a Permian erg on the western margin of Pangea: Depositional system of the Kungurian (late Leonardian) Castle Valley and ABSTRACT known basement ages in the nearby Uncompahgre uplift. In contrast, the Cas- White Rim sandstones and subjacent Cutler Group, Paradox Basin, Utah, USA: Geosphere, v. 11, no. 5, tle Valley Sandstone ranges from quartz-rich arkose to subarkose and exhibits p. 1475–1506, doi:10.1130/GES01174.1 Consideration of petrographic and U-Pb provenance data and paleocurrent a consistent upsection decrease in feldspar content, from Qt71F27L2 in the lower

analysis of Kungurian (upper Leonardian) Cutler Group strata in the salt anti- eolianite member to Qt90F10L0 in the upper member. Like the underlying fluvial Received 3 February 2015 cline province of the Paradox Basin of Utah demonstrates striking contrasts in arkose, the lower eolianite member contains potassium feldspar, plagioclase, Revision received 17 April 2015 composition and inferred sources of stratigraphically adjacent eolian and flu- and mica derived from the Uncompahgre uplift, but the locally derived zircon Accepted 18 June 2015 Published online 5 August 2015 vial facies. Eolian strata, termed here the Castle Valley Sandstone, exposed in age groups constitute only 23%–37% and 13% of the zircon grain ages in the the Castle Valley northeast of Moab, Utah, and long correlated with the White lower and upper eolianite members, respectively; whereas older Archean and Rim Sandstone, were deposited on the southwestern flank of a NW-trending Paleoproterozoic grains, including ca. 1.5 Ga grains uncommon in the Lauren- diapiric salt wall. The eolian strata, which overlie red fluvial sandstone and tian detrital-zircon record, and Grenville, Neoproterozoic, and early Paleozoic conglomerate of the undifferentiated Cutler Formation, are as much as 183 m grains constitute the bulk of the zircons. Quartzarenite of the greater White thick in outcrop and consist of two eolianite members separated by a thin Rim erg contains detrital-zircon populations similar to those of the upper eo- sheet-flood deposit that contains pebbles derived from the salt wall and up- lianite member. The Grenville and younger grains are interpreted as having turned conglomeratic strata adjacent to it. Both eolian and underlying fluvial an eastern Laurentian (Appalachian) source, whereas the ca. 1.5 Ga grains deposits thin and onlap eastward onto the now-collapsed salt wall. Fluvial probably had an ultimate source in Baltica. Sediment-transport directions strata at Castle Valley and in exposures to the northeast were transported indicate that zircon grains not directly attributable to local basement of the northwestward, parallel to the salt wall. Large-scale foresets in the lower eo- Ancestral Rocky Mountains, including grains with a likely Baltica source, were lianite member indicate dominant northeasterly wind directions (present co- transported to the western shoreline of Laurentia by transcontinental fluvial ordinates) and transport directly away from the contemporary Uncompahgre systems and then southeastward to their depositional site at the erg margin uplift, whereas foresets in the upper member indicate variable northeasterly in salt-withdrawal minibasins. and northwesterly paleowinds. The eolian strata thus accumulated on the lee side of the salt wall, but sandstone composition and northwesterly wind components indicate net transport from the northwest, comparable with domi- INTRODUCTION nant southeastward sand transport, away from the Pangean shoreline, documented for the greater White Rim erg to the west and northwest. The NW and The nature of late Paleozoic dispersal systems that delivered sediment to NE winds are both predicted by late Paleozoic atmospheric circulation models the western edge of Pangea and sources of sediment carried by those systems for western Pangea. have been topics of speculation and debate since the earliest paleogeographic

Cutler fluvial sandstones are compositional arkoses (mean Qt56F42L2) con- reconstructions of the supercontinent. Enormous volumes of eolian sediment, taining basement-derived detrital components that include potassium feld- which presumably required aerially extensive source areas and possibly trans- For permission to copy, contact Copyright spar, plagioclase, biotite, and zircons with a restricted, bimodal age distribu- continental sediment-delivery routes, accumulated along the western conti- Permissions, GSA, or [email protected]. tion of ~1790–1689 Ma and ~1466–1406 Ma. These grain ages exactly match nental margin during Late Pennsylvanian and Early Permian time (Blakey et al.,

1988; Johansen, 1988; Marzolf, 1988; Peterson, 1988; Dickinson and Gehrels, The intracratonic Ancestral Rocky Mountain deformation event accompanied 2003). Large erg systems that developed in Early Permian (Wolfcampian and supercontinent assembly and created basement uplifts that provided coarse late Leonardian or Sakmarian–Artiniskian and Kungurian) time along the arkosic sediment to adjacent sedimentary basins in the present region of the NNE-trending shoreline of Pangea (Permian coordinates; Fig. 1) are inferred to Rocky Mountains and Colorado Plateau (Fig. 1; Melton, 1925; Ver Wiebe, 1930; have been fed by littoral sand of the western marine margin (e.g., Blakey et al., Baker et al., 1933; Mallory, 1972a; Kluth and Coney, 1981; Kluth, 1986; Bar- 1988; Dubiel et al., 1996; Condon, 1997; Dickinson and Gehrels, 2003). Many beau, 2003). At the same time, Alleghenian and Ouachita deformation was potential bedrock sources for sediment existed in Pangea due to the wide ex- only recently completed as a result of diachronous collision and terrane ac- tent of deformation that took place during the assembly of the supercontinent: cretion along what had been the eastern and southern flanks of Laurentia

120° W Kungurian shoreline 100° W

20° N

n 0 km 1000

n Wood Havallah basi River basin Antler oroge e Ely Oquirrh basin basin ~10° N Latitud PartlyMississippian emergent topography of Figure 1. Paleogeographic map of 2 Centr 20° N F Pennsylvanian–Permian Ancestral Emery al CO troughro nt Rocky Mountain province. Locations uplift Ran of uplifts and basins adapted from Uncompahgr g e Kluth and Coney (1981), Geslin (1998), u anscontinental arch Bird p Tr 5 lif Barbeau (2003), Dickinson and Law- Spring t basin 4 e ton (2003), and Trexler et al. (2004). Paradox Location and trend of Kungurian basin 6 uplift (late Leonardian) shoreline from the 1 3 Taos trough Kungurian 275 Ma paleogeographic map on the Fig. 3 shoreline Colorado Plateau Geosystems Web ~10˚ N Latitude Location site (cpgeosystems.com /nam .html), last accessed January 2015. Predicted Zuni Sierra Amarillo-Wichita uplift wind directions and paleolatitudes for Grande uplift Anadarko basin uplift late Paleozoic from Parrish and Peter- continental arch ns son (1988) and Peterson (1988). Bold 120° W ra 110° W T Orogrande numerals are locations of stratigraphic Matado basin r columns of Figure 2. Explanation of Late Paleozoic Paleogeographic arch Elements and Predicted Pangean Wind Directions Pedernal uplift Central Basement uplift exposed Zonal (trade) Diablo Basin in Kungurian time wind direction platform platform Basement uplift or arch onlapped by lower Alternate Pedregosa Permian strata monsoonal basin Pennsylvanian wind direction r sedimentary basin Kungurian 30° N shoreline Approximate Equato Pennsylvanian-Early Permian sedimentary Deformation front of 1 Correlation chart basin location (Fig. 2) Laurentia-Gondwana suture

(Hatcher, 1989; Viele and Thomas, 1989; Keller and Hatcher, 1999), and accre- 1981). The Paradox Formation is overlain by, and grades southwestward into, tion of exotic terranes had recently affected the Cordilleran margin of Laurentia mixed carbonate and siliciclastic strata of the Honaker Trail Formation, which (Speed and Sleep, 1982; Wright and Wyld, 2006). Therefore, discrimination of records glacio-eustatic fluctuations driven by Milankovitch cyclicity (Gold potential sources for late Paleozoic eolian sediment has important implications hammer et al., 1994). The Paradox Formation grades to coarse-grained silici- for Pangean paleogeography and sediment-transport systems and informs clastic strata of the undifferentiated Hermosa Group on the northeast flank of general models for eolian sediment supply and accumulation. the basin (Dubiel et al., 2009). The Cutler Formation overlies the Honaker Trail This paper describes the structural and depositional settings of continental Formation and consists of undifferentiated alluvial and fluvial arkose and con- deposits of the Permian Cutler Group in and near Castle Valley, Utah, located glomerate as much as 2450 m thick in the proximal northeastern part of the ba- in the proximal part of the Paradox Basin, and compares the petrography and sin near the Uncompahgre uplift (Condon, 1997; Doelling, 2002a; Venus et al., detrital-zircon content of these deposits to correlative eolian strata of the White 2015). Proximal fluvial strata of the Cutler Formation in the northeastern part Rim Sandstone of the more distal basin to the southwest. The data presented of the basin have been differentiated on the basis of unpublished, proprietary here provide insight into sediment sources and sediment-transport systems seismic data (Trudgill, 2011). The upper part of the undifferentiated Cutler For- for voluminous Lower Permian eolian deposits as well as continent-scale mation has been identified as the Organ Rock Formation (Rasmussen, 2009, paleogeography of Laurentia in its broader context within Pangea. 2014), a formal term applied to red continental strata overlying eolian strata of the Cedar Mesa Sandstone and underlying the eolian White Rim Sandstone in the central and southwestern parts of the basin (Fig. 2; Baars, 1962; Stanesco GEOLOGIC SETTING et al., 2000; Dubiel et al., 2009); however, the eolian units, particularly the Cedar Mesa Sandstone, that permit unambiguous identification of the Organ Upper Leonardian (Kungurian) clastic strata of the Paradox Basin, which Rock Formation are absent from most outcrops of the proximal part of the include the White Rim Sandstone and its correlatives, were deposited late in basin. Because of persisting uncertainty regarding correlation, the term, un- the history of the Ancestral Rocky Mountains deformational event, an episode differentiated Cutler Formation, is retained in this paper for fluvial and allu- of regional crustal deformation that created yoked basement-cored uplifts vial facies of the basin northeast of Moab, Utah. The undifferentiated Cutler and basins extending between Oklahoma and Nevada (Fig. 1; Melton, 1925; Formation onlaps and buries the Uncompahgre uplift near Gateway, Colorado Ver Wiebe, 1930; Trexler et al., 2004). During the late Paleozoic, the Ancestral (Figs. 3 and 4; Melton, 1925; Soreghan et al., 2009; Kluth and DuChene, 2009; Rocky Mountains province lay at tropical latitudes, ~10° north of the equator Rasmussen, 2009), where the formation consists of boulder conglomerate (Fig. 1; Scotese et al., 1979; Scotese and McKerrow, 1990; Dubiel et al., 2009), and coarse-grained sandstone generally interpreted as proximal to distal allu- and the climatic regime has been inferred to have ranged from semi-arid in vial-fan deposits (Schultz, 1984; Mack and Rasmussen, 1984). Pennsylvanian time to seasonally wet or even peri-glacial in the Early Permian The undifferentiated Cutler Formation fines southwestward across the (Soreghan et al., 2002, 2009). basin, grading laterally to a succession of formations considered components of the Cutler Group (Fig. 2; Baars, 1962; Condon, 1997). These formations alternate between red-weathering structureless siltstone and fluvial sand- Paradox Basin stone and siltstone represented by the Halgaito Formation (or “lower Cutler beds”), which overlies the Honaker Trail Formation, and the younger Organ The northwest-trending Paradox Basin contains an asymmetric sedimen- Rock Formation (e.g., Langford and Chan 1988, 1989; Condon, 1997; Stan- tary fill that thickens northeastward toward the basement-cored Uncompahgre esco et al., 2000; Soreghan et al., 2002; Mountney and Jagger, 2004) and uplift. The basin is interpreted as the result of flexural subsidence adjacent visually striking, thick-bedded white to pink eolian sandstone intervals that in- to the basement load (Barbeau, 2003; Trudgill, 2011), and a number of faults clude the Cedar Mesa Sandstone and younger White Rim Sandstone (Loope, within the uplift and flanking it have demonstrated late Paleozoic sinistral 1984; Huntoon and Chan, 1987; Blakey et al., 1988; Blakey, 1996; Langford and strike-slip or normal movement (Weimer, 1980; Baars and Stevenson, 1981; Chan, 1988; Chan, 1989; Dubiel et al., 1996, 2009). Arkosic composition and Stevenson and Baars, 1986; Thomas, 2007). The basin is defined by the dis- southwest-fining trends of fluvial strata of the undifferentiated Cutler Group tribution of Pennsylvanian and Permian strata included in the Paradox For- and the Organ Rock Formation have led to the generally accepted view that mation, Honaker Trail Formation, and Cutler Group in Utah and the Hermosa basement rocks of the Uncompahgre uplift were the primary source of the Group and Cutler Formation in Colorado (Figs. 2 and 3). The Paradox Forma- fluvial sediment (Ver Wiebe, 1930; Baars, 1962; Cater and Elston, 1963; Mal- tion is a cyclic succession of shale, dolomite, and basin-central evaporite as lory, 1972a, 1972b; Campbell, 1979, 1980; Kluth and Coney, 1981; Kluth, 1986; much as 4300 m thick (Baker et al., 1933; Hite, 1970; Hite and Buckner, 1981; Condon, 1997; Barbeau, 2003; Blakey, 2009). Sediment in the eolian intervals Doelling, 2002a). Evaporites within the cycles include gypsum, anhydrite, was largely derived from coastal sand at the edge of the Permian seaway to halite, carnallite, and sylvite (Hite, 1970; Hite et al., 1972; Hite and Buckner, the west and northwest (Kamola and Chan, 1988; Dubiel et al., 1996, 2009;

Ma AGE 1. Grand 2. 3. 4. Distal 5. Proximal 6. Proximal Canyon SE Oquirrh Monument Paradox Paradox Paradox ICS N. America Region Basin Valley Basin Basin, UT Basin, CO Olenekian Moenkopi Thaynes Moenkopi Moenkopi 250 ias Earl y Tr Induan Woodside Changhsing.

Lat e Wuchiaping. Ochoan

260 Figure 2. Correlation chart for upper Capitanian Capitanian Paleozoic formations of the Paradox

e Basin and vicinity, southwestern Lau- rentia, including: (1) the Grand Canyon iddl Park Wordian Wordian region of northern Arizona; (2) the City southeastern flank of the Oquirrh 270 Roadian Roadian Kaibab Kaibab basin in central Utah; (3) Monument ? Valley, on the southern flank of the Toroweap Paradox Basin; (4) the southwestern Diamond Cr White Castle Kungurian Coconino part of the Paradox Basin in SE Utah; Leonardian Rim Valley De Chelly (5) the northeastern part of the Para- Permian Kirkman dox Basin in east-central Utah; and 280 Hermit Organ Organ (6) the southeastern part of the Para Rock Rock dox Basin westernmost Colorado. Artinskian Locations of columns indicated on Cutler, Figure 1. Equivalence of International Earl yM Cutler, undiff. Union of Geological Sciences (IUGS) Esplanade Cedar Cedar and North American Pennsylvanian 290 Wolfcampian Granger undiff. Mountain Mesa Mesa substages from Richards (2013); equiv- Cutler Group Sakmarian Cutler Group alence of Permian stages from Grad- stein et al. (2012). Stippled units indicate major eolian sandstones. Sources Halgaito/ Halgaito/ of data: Baars (1962); Bissell (1962); Asselian Lwr Cutler Lwr Cutler Irwin (1971); Blakey et al. (1988); Hintze 300 Wallsburg (1988); Blakey (1990, 2009); Condon Gzelian Virgilian Wescogame Ridge/ Honaker Honaker Honaker (1997); Dubiel et al. (2009). Precise age Shingle ranges of all eolian units are uncertain. Kasimovian Missourian Mill Hermosa Trail Trail Trail

Oquirrh Group Group Desmoines. Paradox Paradox Paradox 310 Moscovian Bear

Canyon Hermosa Gp . Pinkerton Trl Hermosa Gp . Pinkerton Trl Hermosa Gp . Pinkerton Trl Manakacha

Pennsylvanian Atokan

Carboniferous (part) Bashkirian 320 Morrowan Watahomigi Bridal Veil Falls

Condon, 1997). On the basis of the large volume of eolian sand, its quartz- Formation and finer-grained differentiated stratigraphic entities of the Cutler ose composition, and subsequently on the basis of its detrital-zircon content, Group (Figs. 3 and 4; Baker et al., 1933; Shoemaker et al., 1958; Jones, 1959; ultimate sources in the Appalachian orogen of eastern Laurentia have been Doelling, 1988; Trudgill, 2011). The salt walls developed by rapid diapiric move- posited for sediment of the eolian sandstones (Johansen, 1988; Marzolf, 1988; ment of Paradox Formation evaporite during Late Pennsylvanian, Permian, Dickinson and Gehrels, 2003). and Triassic time; salt migration continued at slower rates in the Jurassic and A belt of salt walls cored by Paradox evaporite, termed the salt anticline Cretaceous (Doelling, 1988, 2002a; Trudgill, 2011). Evidence for syndeposi- province, occupies the thick proximal part of the Paradox Basin and forms tional salt rise includes thinning of strata and angular unconformities on the a broad region of transition between coarse-grained undifferentiated Cutler flanks of diapiric structures (Shoemaker et al., 1958; Jones, 1959; Elston et al.,

Explanation 108º W 110º W Map Area Laramide uplift Uncompahgre Eagle Basin Extent of Late Paleozoic Uncompahgre uplift R. Distribution of salt in Paradox Formation Lower Permian on San Rafael Proterozoic Colorado Re Proterozoic outcrop in Swell GJ 0 100 km Uncompahgre uplift 39º N GR and San Juan dome Gunnison UC Green SA Jurassic on Central Colorado Diapiric salt walls 11CT01 CH FV Proterozoic Al Structural culminations Gw R. Mo SV BC indicated by exposed R. 11WRA CV Triassic on Trough evaporite or collapsed Proterozoic Mn roof strata MV Circle Cliffs LIC PV Lower Permian Crestone- Subsurface diapir Uplift on Proterozoic Sand Creek indicated by gravity LV ? ? fault system Paradox BasinGV Ou 38º N data River Dolores ? Lower 11WRB Uplift Cr Detrital zircon locality Paleozoic on Hite Proterozoic 11WRB not on Castle Valley Map (Figure 5) R. Limit of Paradox NM Community Colorado Evaporite Reverse fault on San Juan n Juan River structural front of ND Sa Dome Uncompahgre uplift Du Colorado Inferred basement Utah MH onlap limits of 37º N New Mexico Paleozoic & Mesozoic Arizona 110º W Systems, as indicated 108º W 106º W

Figure 3. Location map of Paradox Basin, Uncompahgre uplift, Laramide uplifts flanking the Paradox Basin, Proterozoic outcrops within the Paleozoic and Laramide uplifts, and locations described in text. Paradox Basin is defined by extent of evaporite facies, generalized from Condon (1997) and Stevenson and Wray (2009), but Permian siliciclastic rocks extend well beyond indicated limits of basin. Extent of Uncompahgre uplift modified from numerous sources including DeVoto (1980), Weimer (1980), Hoy and Ridgway (2002), and Barbeau (2003), as described in text. Rectangle spanning Utah-Colorado state line indicates area of Figure 4. Communities: Al—Almont; Cr—Crestone; Du—Durango; GJ—Grand Junction; GR—Green River; Gw—Gateway; MH—Mexican Hat; Mn—Montrose; Mo—Moab; Ou—Ouray; Re—Redstone. Localities: BC—Black Canyon of the Gunnison River; ND—Nokai Dome; NM—Needle Mountains; UC—Unaweep Canyon. Salt walls of salt anticline province: CH—Cache Valley; CV—Castle Valley; FV—Fisher Valley (aka Onion Creek diapir); GV—Gypsum Valley; LV—Lisbon Valley; MV—Moab Valley; PV—Paradox Valley; SA—Salt Valley; SV—Sinbad Valley; LIC—Paleogene intrusive complex of La Sal Mountains.

1962; Cater and Elston, 1963; Trudgill et al., 2004; Matthews et al., 2004; Law- interbeds to shallow levels in the diapirs; thus, local diapir exposure is indi- ton and Buck, 2006; Trudgill, 2011) and fluvial sediment transport parallel to cated by conglomerate beds near several of the salt walls containing clasts of the axes of salt-withdrawal “minibasins” formed by the migration of evaporite Paradox carbonate and less common gypsum eroded from the exposed salt into the diapiric structures (Matthews et al., 2004; Banham and Mountney, walls and deposited in Permian and Triassic strata (Shoemaker et al., 1958; 2013, 2014). Rising Paradox evaporite entrained blocks of dolostone and shale Elston et al., 1962; Lawton and Buck, 2006).

300 Explanation 0 Mobil Xb Xb #1 McCormick Uncompahgre GJ Uplif Geologic Units GR 39° N Xg 0 Gunnis Pgi Paleogene intrusive rocks 400 Mobil Green R. 100 Yg Extent of Permian White #1-30 o 100 Pure Oil n Rim Sandstone and related Gateway #1 R. units (isopachs in feet) G t Permian strata overlie r 400 SA Yg Yg basement rocks of uplift e a O&G #1 Xb t Mobil #1-7 Triassic & Jurassic strata e CH State YXg r UC overlie basement rocks

of uplift Exxon #1 W YXg YXg Paleoproterozoic Moab Fig.5 Gw Xb metamorphic rocks h Salt FV i fault t 500 (~1.8–1.7 Ga) e 100 CV

Paleoproterozoic (~1.7– AnticlineSV Provinc YXg Xg 1.6 Ga) granitic rocks R 200 0 Burk i Pgi m Paleoproterozoic and Mo 200 SD YXg Mesoproterozoic

granitic rocks undivided 0 Pgi e YXg Mesoproterozoic (~1.4 Ga) r MV g Yg granitic rocks, commonly 25 CC megacrystic Pgi e 700 La Sal Diapiric salt walls intrusive Structural culminations complex PV indicated by exposed evaporite or collapsed roof strata 500 0 Paradox Basin Subsurface diapir LV indicated by gravity data 300

Other Symbols Dirty Devil R. Colorado R. GV Reverse fault on structural front of Uncompahgre uplift Dolores R. Paleocurrent direction 38° N from eolian foresets,White

Rim and Castle Valley 0 sandstones 100 Paleocurrent direction 0 100 km from trough cross-bed 110° W axes, Cutler fluvial facies Hite

Figure 4. Map showing thickness of White Rim Sandstone and correlative strata in Salt anticline region (isopachs in feet), paleocurrent data from eolian strata and fluvial strata roughly correlative with Organ Rock Formation, and distribution of Proterozoic rocks in Uncompahgre uplift. Labels as in Figure 3 and CC—Cane Creek anticline; SD—Shafer Dome. Thickness data, adapted from Baars and Seager (1970), Condon (1997), Trudgill (2011), and Parr (2012), indicate strong influence of salt-withdrawal minibasins southwest of Salt Valley (SA), Castle Valley (CV), and Moab Valley (MV) salt walls on thickness and orientation of Kungurian erg margin. Paleocurrent data from Baars and Seager (1970), Huntoon and Chan (1987), Buller (2009), Venus et al. (2015), and this study. Basement rock units from Tweto (1979) and Doelling (2002a). Dashed rectangle at NW end of Castle Valley salt wall indicates location of Figure 5. Oil well symbols indicate selected wells that indicate subcrop relations near structural front of Uncompahgre uplift and key thickness localities of eolian strata at top of Cutler Group, explained in text.

Uncompahgre Uplift the southwestern part of the Uncompahgre uplift near Ouray, Colorado; to the south in the San Juan dome north of Durango, Colorado; in the northwestern The Uncompahgre uplift, which lay along the northeastern margin of the part of the uplift in Unaweep and Black canyons; in the vicinity of Almont, Colo Paradox Basin, was a doubly vergent basement-involved uplift as much as rado, on the northeastern side of the uplift; and in the Colorado River canyon 160 km wide with marked, but as-yet undetermined, topographic relief (Figs. west of Grand Junction, Colorado (Fig. 3). 1 and 3; DeVoto, 1980; Hoy, 2000; Hoy and Ridgway, 2002). Seismic data and Following late Paleozoic uplift, the Uncompahgre uplift was reactivated and drilling indicate that basement rocks are thrust southwestward over Pennsyl- its structures overprinted by Laramide shortening, which resulted in the devel- vanian and Permian strata, generally synorogenic clastic deposits, near the opment of reverse faults and monoclinal folds (Lindsey et al., 1983); it was then mountain front, in Utah (Fig. 1; Mobil #1 McCormick well; Frahme and Vaughn, buried by Paleogene volcanic and volcaniclastic rocks and cut by normal faults 1983) and possibly over salt of the Paradox Formation in southwestern Colo- and sediment-filled grabens of the Neogene Rio Grande rift (Tweto, 1979; Hoy rado (Kluth and DuChene, 2009). Frontal structures on the southwestern side and Ridgway, 2002). These younger events and features have created uncer- of the Uncompahgre uplift are extensively buried beneath Permian and Trias- tainty as to the stratigraphic and structural relations unique to the Paleozoic sic clastic rocks, but exposed reverse faults of Pennsylvanian–Permian age em- history of the uplift, and even as to its Paleozoic extent (compare Baars, 1966; place basement rocks over Pennsylvanian and Permian conglomerate of the Condon, 1997; Hoy and Ridgway, 2002; Barbeau, 2003; Thomas, 2007). Central Colorado trough on the northeast flank of the uplift (Fig. 3; Hoy, 2000; Hoy and Ridgway, 2002). Alluvial-fan facies of the Permian Maroon Formation directly west of Redstone, Colorado, on the northeast flank of the uplift, indi- Stratigraphic Relations and Age of the White Rim Sandstone cate a nearby boundary between the uplift and the Eagle basin (Fig. 3). Base- ment rocks on the southwest flank of the uplift are overlain by the upper part of Throughout its geographic distribution, the White Rim Sandstone lies at the Cutler Formation near Gateway, Colorado, and along the frontal part of the the top of the Cutler Group. It overlies fluvial strata of the Organ Rock Forma- uplift (Soreghan et al., 2009), by Triassic beds of the Chinle Formation along tion on a sharp contact interpreted as a sequence boundary (Blakey, 1996) the Colorado River and southeastward along the uplift (Tweto, 1979; Doelling, and is unconformably overlain by the Moenkopi Formation. The White Rim 2002a), and Jurassic strata in the vicinity of the Black Canyon of the Gunnison Sandstone interfingers westward with the fossiliferous Toroweap Formation, River to the northeast (Fig. 3; Tweto, 1979). The distribution of strata deposited which establishes its age as late Leonardian (late Kungurian; Fig. 2; Irwin, 1971; on Proterozoic rocks therefore demonstrates progressive northeastward onlap Blakey et al., 1988; Blakey, 1996). On the eastern flank of the Circle Cliffs uplift of basement perpendicular to the mountain front well into Mesozoic time and and the San Rafael Swell (Fig. 3), the White Rim also interfingers with the indicates that Uncompahgre basement was extensively exposed during the lower part of the Kaibab Limestone, the age of which is poorly known, and Permian. Farther southeast, on the San Juan dome of Laramide age, Protero on the San Rafael Swell, the White Rim is overlain by the upper part of the zoic rocks are overlain by a thin veneer of Cambrian–Mississippian strata and a Kaibab, which is of Wordian age (Fig. 2; Irwin, 1971; Huntoon and Chan, 1987; thick succession of Pennsylvanian rocks (Tweto, 1979; Weimer, 1980; Thomas, Kamola and Chan, 1988). The Kaibab Limestone is not present along the Green 2007) and thus were not exposed during Pennsylvanian and Permian time. and Colorado Rivers, and the upper surface of the White Rim Sandstone dis- South of Ouray, Colorado, where the structural front of the Uncompahgre plays irregular topography (Baars and Seager, 1970; Orgill, 1971; Huntoon and uplift appears to be offset by a major basement fault (Fig. 3; Weimer, 1980), Chan, 1987; Kamola and Chan, 1988). Where the top of the White Rim Sand- west-trending faults with demonstrated Pennsylvanian and Permian displace- stone is exposed between the Green and Colorado rivers and west of their con- ment form a system of horsts and grabens south of the main uplift (Baars, fluence, the upper surface of the formation displays numerous linear ridges 1966; Weimer, 1980; Thomas, 2007). 3–5 m high that trend NNW and are asymmetric with steeper west flanks; the Pre-Pennsylvanian rocks of the Uncompahgre uplift consist of metamor- most prominent of these ridges is 75 m high and trends NE (Baars and Seager, phosed volcanic, plutonic, and sedimentary rocks intruded by posttectonic 1970; Huntoon and Chan, 1987). These ridges were initially interpreted as elon- granites and overlain by a thin cratonic succession of Cambrian–Mississip- gate marine bars oriented parallel with a dominant SSE transport direction pian strata. Paleoproterozoic rocks include foliated granites and metavolcanic indicated by large-scale foreset dips (Baars and Seager, 1970), an interpreta- rocks with U-Pb ages ranging 1.78–1.69 Ga (Silver and Barker, 1968; Bickford tion contravened by subsequent eolian interpretation of the White Rim Sand- et al., 1989; Gonzales and Van Schmus, 2007), which are overlain by quartz- stone (Huntoon and Chan, 1987; Chan, 1989; Dubiel et al., 1996, 2009). The ite and phyllite with maximum depositional ages near 1.67–1.65 Ga (Jessup topographic features were subsequently attributed to both erosional sculpt- et al., 2006; Jones et al., 2009). The metasedimentary succession is folded ing of uppermost White Rim strata and preservation of relic dune topography and intruded by porphyritic Mesoproterozoic granitoids with U-Pb ages near during peak transgression of the Kaibab seaway (Huntoon and Chan, 1987; 1.44 Ga (Silver and Barker, 1968; Bickford and Cudzilo, 1975; Gonzales and Chan, 1989), which suggests that the White Rim Sandstone is entirely older Van Schmus, 2007). Basement rocks of these ages are presently exposed in than the upper part of the Kaibab Limestone in the vicinity of the Colorado and

Green rivers. The chronostratigraphic correlation of Figure 2 illustrates a Kun- sured in fluvial strata of the Cutler fluvial beds along Onion Creek northeast gurian (Leonardian) age for the top of the White Rim Sandstone, as depicted of Castle Valley and at locations on the flanks of Castle Valley (Buller, 2009). by Blakey et al. (1988), although the sandstone may contain Roadian (formerly Petrographic and detrital-zircon samples were collected within the map area of Guadalupian) strata to the west where it interfingers with the Kaibab Lime- Figure 5 and elsewhere in the basin, as described later. stone. The White Rim Sandstone is equivalent to the little-studied Diamond Standard petrographic thin sections stained for potassium feldspar were Creek Sandstone, as much as 305 m thick, of north-central Utah (Irwin, 1971; counted using the Gazzi-Dickinson technique to minimize compositional de- Hintze, 1988), which was deposited along the southeastern flank of the Oquirrh pendency on grain size (Ingersoll et al., 1984). Four hundred framework grains basin adjacent to the Permian seaway (Figs. 1 and 2) and is interpreted as an were counted per sample to achieve a 2s confidence of ±5% (Van der Plas and eolian deposit (Bissell, 1962). Detrital-zircon data described below suggest that Tobi, 1965). Sandstone modal compositions are listed in stratigraphic order the Diamond Creek Sandstone formed part of the greater White Rim erg. in Table 1. The White Rim Sandstone thins eastward, counter to the thickness trend Zircon separates from Permian strata were analyzed using a laser-ablation, of the undifferentiated Cutler Formation, to a well-defined, exposed pinch inductively-coupled plasma mass spectrometer (LA-ICP MS) at the University out along the present Colorado River southwest of Moab (Fig. 4; Baars, 1962; of Arizona LaserChron Center. Zircons were separated using standard min- Baars and Seager, 1970; Condon, 1997). Eolian sandstone is not widely re- eral separation techniques. Approximately 100 individual zircon analyses were ported from outcrops east of the pinch out, but thick-bedded sandstone, gen- conducted per detrital sample. Analytical errors and procedures are described erally identified as White Rim, is present in the subsurface along the west flank elsewhere (Gehrels et al., 2008; Gehrels, 2012). A 90%–110% concordance filter of the Moab Valley salt wall and on both flanks of the Salt Valley salt wall (Fig. 4; was applied to the zircon-grain analyses; the filter resulted in rejection of 2% Trudgill, 2011; Rasmussen, 2014). Thick-bedded, reddish-orange, fine-grained of the grains from the detrital-grain suite. Rejected grain ages are indicated by sandstone with large-scale planar cross-beds and abundant rounded medium strike-through text in Supplemental Table 11. In this paper, we employ the 2012 grains, a textural characteristic of the White Rim Sandstone and other Permian GSA Time Scale (Walker et al., 2012). eolianite units of the Paradox Basin, is present in the uppermost 34–74 m of the undifferentiated Cutler Formation adjacent to the Moab fault (Doelling, 1988), which marks the northwestward projection of the Moab Valley salt wall (Fig. 4). STRATIGRAPHY AND STRUCTURAL GEOLOGY A conspicuous outcrop of eolian sandstone, the topic of this study, forms a OF CASTLE VALLEY

Supplemental Table 1. U-Pb geochronologic analyses of detrital zircons in Permian strata of Paradox Basin. Isotope ratiosApparent ages (Ma) AnalysisU206PbU/Th206Pb* ±207Pb* ±206Pb* ±error 206Pb* ±207Pb*±206Pb* ±Best age ± Conc prominent cliff on the southwestern flank of the Castle Valley salt wall, where (ppm)204Pb207Pb* (%)235U*(%) 238U (%)corr. 238U* (Ma) 235U (Ma) 207Pb* (Ma) (Ma) (Ma) (%)

11WR-A White Rim Sandstone at base of Shafer Trail, Canyonlands National Park. 38° 27.616' N, 109° 47.653' W 11WR-A-17 541344150.7 18.77713.1 0.3487 3.90.04752.3 0.59 299.16.7 303.710.2339.8 70.9 299.16.7 98.5 11WR-A-90 660935221.6 18.66801.0 0.3763 1.60.05091.3 0.79 320.34.1 324.34.6 352.922.6320.3 4.1 98.8 the sandstone occupies a position between fluvial strata of the undifferentiated The northwestern end of Castle Valley contains superb exposures of Cutler 11WR-A-5 85 116300.9 18.715512.40.424912.50.05771.5 0.12 361.45.4 359.537.9347.1 281.5 361.45.4 100.5 11WR-A-74 4034704 1.414.6258 21.6 0.5686 22.2 0.0603 4.90.22377.5 17.9457.1 81.8 879.8 452.6 377.5484 17.9 82.6 11WR-A-52 263465291.6 18.50982.7 0.4539 3.00.06091.2 0.40 381.34.4 380.09.5 372.161.9381.3 4.4 100.3 11WR-A-95 177269630.9 18.41682.9 0.4891 3.50.06531.9 0.55 407.97.6 404.311.7383.4 66.0 407.97.6 100.9 11WR-A-3 135226722.3 18.20644.9 0.4982 5.40.06582.2 0.41 410.78.7 410.518.1409.2 109.3 410.78.7 100.1 11WR-A-61 258105046 1.318.1133 4.70.51024.9 0.0670 1.50.30418.2 6.0418.6 16.9 420.6 105.0 418.26.0 99.9 Cutler Formation and the Moenkopi Formation. Many workers have regarded Group strata and geometric relations that are the keys to understanding the 11WR-A-20 261447071.7 17.83672.7 0.5239 2.90.06781.1 0.39 422.74.5 427.710.1454.9 59.0 422.74.5 98.8 11WR-A-80 359352455.8 18.08051.6 0.5222 2.30.06851.6 0.70 427.06.7 426.68.0 424.736.5427.0 6.7 100.1 11WR-A-31 124293524.9 18.88715.4 0.5083 6.10.06962.7 0.44 434.011.1417.3 20.7 326.5 123.7 434.011.1 104.0 11WR-A-30 299340921.2 17.94632.6 0.5354 2.90.06971.1 0.40 434.34.8 435.410.1441.3 58.3 434.34.8 99.7 11WR-A-18 140368120.9 17.18355.2 0.6855 5.70.08542.4 0.42 528.5 12.2530.1 23.6 537.1113.3528.5 12.2 99.7 this exposed eolian unit as an outlier of the White Rim Sandstone (e.g., Dubiel interaction of the strata with the developing salt wall, controls on facies distri- 11WR-A-89 296688561.8 17.08591.4 0.7343 4.40.09104.2 0.95 561.4 22.4559.1 18.8 549.629.6561.4 22.4 100.4 11WR-A-66 68 155761.9 16.52675.7 0.7670 5.90.09191.3 0.22 566.96.9 578.025.8621.8 123.3 566.96.9 98.1 11WR-A-24 112188211.4 17.13663.7 0.7557 4.10.09391.9 0.45 578.7 10.3571.6 18.1 543.180.7578.7 10.3 101.3 11WR-A-12 128385870.9 17.22893.6 0.7751 3.90.09691.4 0.35 595.97.8 582.717.1531.4 79.1 595.97.8 102.3 11WR-A-48 213337084.2 16.16893.8 0.8350 4.30.09792.0 0.47 602.211.7616.4 19.8 668.880.9602.2 11.7 97.7 11WR-A-82 142251941.0 16.82644.3 0.8077 4.50.09861.5 0.33 606.08.7 601.220.5582.9 92.4 606.08.7 100.8 et al., 1996, 2009; Condon, 1997; Doelling and Ross, 1998; Doelling, 2002a; bution, and sources of sediment for the Cutler Group (Fig. 5). The Castle Valley 11WR-A-23 344798541.7 16.78501.2 0.8098 1.80.09861.3 0.72 606.17.3 602.38.0 588.226.8606.1 7.3 100.6 11WR-A-67 44 9178 0.715.9699 8.10.90118.8 0.1044 3.50.40640.0 21.4652.3 42.4 695.3 172.1 640.021.4 98.1 11WR-A-60 337854722.5 15.89681.1 1.0175 1.60.11731.2 0.74 715.08.2 712.68.4 705.123.8715.0 8.2 100.3 11WR-A-84 122403203.0 14.00452.9 1.5285 3.10.15521.1 0.37 930.39.8 941.918.9969.1 58.4 969.158.4 98.8 11WR-A-42 191716172.8 13.60991.1 1.8241 2.40.18012.1 0.89 1067.3 21.0 1054.215.81027.122.61027.122.6 101.2 11WR-A-94 159572952.5 13.52890.9 1.8364 1.80.18021.5 0.86 1068.0 14.9 1058.611.61039.218.21039.218.2 100.9 Huntoon et al., 2002), and interpretation of subsurface data indicates that the Sandstone and undifferentiated Cutler Formation are described briefly with 11WR-A-7 59 243391.6 13.48283.5 1.7575 3.80.17191.3 0.35 1022.4 12.5 1029.924.41046.171.11046.171.1 99.3 11WR-A-56 146122347 1.613.4736 1.51.83881.9 0.1797 1.20.63 1065.3 12.1 1059.412.81047.530.31047.530.3 100.6 11WR-A-4 233146023 1.613.4689 1.71.82352.9 0.1781 2.40.82 1056.7 23.7 1053.919.31048.133.61048.133.6 100.3 11WR-A-59 169688996.7 13.43441.3 1.7987 2.20.17531.8 0.82 1041.0 17.5 1045.014.51053.325.61053.325.6 99.6 11WR-A-91 48 197651.2 13.35336.5 1.8469 6.70.17891.9 0.28 1060.8 18.6 1062.344.41065.5 130.1 1065.5 130.1 99.9 Castle Valley exposure connects directly with the White Rim Sandstone of the other local stratigraphic units in the following section, and in more detail in the 11WR-A-93 28 9641 1.013.3292 7.31.85877.6 0.1797 2.00.26 1065.2 19.2 1066.550.21069.1 147.8 1069.1 147.8 99.9 11WR-A-6 116548722.8 13.24302.5 1.9129 2.90.18371.4 0.49 1087.3 14.1 1085.619.31082.150.61082.150.6 100.2 11WR-A-86 310829675.8 13.23181.3 1.8004 7.40.17287.3 0.98 1027.4 69.5 1045.648.61083.826.91083.826.9 98.3 11WR-A-79 178660722.5 13.23151.1 1.9015 2.30.18252.1 0.89 1080.5 20.7 1081.615.61083.921.31083.921.3 99.9 11WR-A-71 46 179721.8 13.20113.3 1.9012 5.10.18203.9 0.77 1078.1 39.1 1081.534.21088.566.21088.566.2 99.7 11WR-A-96 49 463861.8 13.14803.7 1.9139 4.60.18252.6 0.57 1080.7 26.1 1085.930.41096.674.81096.674.8 99.5 greater erg via the salt-withdrawal basin that lies between the Moab and Salt section on sedimentology. 11WR-A-68 357145631 3.013.1308 0.71.97851.5 0.1884 1.30.881112.8 13.51108.210.11099.214.21099.214.2 100.4 11WR-A-73 76 390371.8 13.12173.5 1.9204 4.20.18282.3 0.55 1082.0 23.1 1088.227.91100.669.51100.669.5 99.4 11WR-A-98 1755419013.512.9748 1.22.06152.7 0.1940 2.40.891142.9 25.31136.118.61123.024.71123.024.7 100.6 11WR-A-25 275120006 2.312.8972 0.42.05741.2 0.1924 1.20.951134.6 12.31134.78.5 1135.07.8 1135.07.8 100.0 11WR-A-51 154737981.6 12.81230.9 2.0638 1.50.19181.2 0.81 1131.0 12.71136.910.41148.117.81148.117.8 99.5 Valley salt walls (Fig. 4; Trudgill, 2011; Parr, 2012). Due to the absence of di- 11WR-A-39 57 430432.7 12.37264.2 2.3325 4.40.20931.3 0.31 1225.1 15.1 1222.231.31217.282.41217.282.4 100.2 11WR-A-83 141319721.8 12.31960.8 2.1963 2.10.19621.9 0.92 1155.1 19.91179.914.31225.615.91225.615.9 97.9 11WR-A-27 204577431.8 12.04831.1 2.3610 1.90.20631.6 0.82 1209.1 17.5 1230.913.81269.221.91269.221.9 98.2 11WR-A-12 91 393972.4 11.96812.1 2.5830 4.10.22423.6 0.87 1304.1 42.2 1295.830.21282.240.21282.240.2 100.6 11WR-A-10 24 155232.3 11.84565.2 2.7457 5.60.23592.0 0.36 1365.3 24.7 1340.941.71302.2 101.6 1302.2101.6 101.8 11WR-A-2 2371143704.4 11.72400.4 2.2925 2.90.19492.9 0.99 1148.0 30.1 1210.020.51322.28.2 1322.28.2 94.9 rect surface connection with the White Rim Sandstone and some uncertainty 11WR-A-53 73 561552.9 11.63351.9 2.8170 2.10.23770.8 0.39 1374.6 10.0 1360.115.61337.237.01337.237.0 101.1 11WR-A-85 60 390783.5 11.60393.0 2.7624 3.80.23252.3 0.60 1347.5 27.7 1345.428.21342.258.31342.258.3 100.2 11WR-A-37 67 468713.2 11.40162.2 2.9339 2.60.24261.3 0.52 1400.2 16.9 1390.719.41376.142.01376.142.0 100.7 11WR-A-58 135858412.7 11.32730.7 2.8881 2.40.23732.3 0.96 1372.5 28.5 1378.818.11388.613.21388.613.2 99.5 11WR-A-77 1531103602.1 11.11090.9 3.0178 1.70.24321.4 0.83 1403.2 17.4 1412.112.71425.617.71425.617.7 99.4 regarding correlation with other Permian eolian deposits discussed later, the 11WR-A-9 100775320.7 10.98321.8 3.1214 3.70.24863.2 0.87 1431.5 41.4 1438.028.41447.634.51447.634.5 99.5 General Stratigraphy 11WR-A-44 125133297 1.810.7885 1.13.33531.5 0.2610 1.10.71 1494.8 14.2 1489.411.71481.620.01481.620.0 100.4 11WR-A-69 127253001.6 10.72100.9 3.4036 5.70.26475.6 0.99 1513.6 75.3 1505.244.41493.517.91493.517.9 100.6 11WR-A-62 142374913 1.710.6814 0.83.32552.2 0.2576 2.10.94 1477.7 27.2 1487.117.11500.514.21500.514.2 99.4 11WR-A-72 2201136802.1 10.48441.8 3.4514 2.30.26241.3 0.59 1502.3 17.8 1516.217.81535.634.31535.634.3 99.1 11WR-A-81 67 417093.3 10.32152.8 3.8528 3.20.28841.6 0.49 1633.6 23.0 1603.926.11565.052.91565.052.9 101.9 eolian strata of Castle Valley are here named the Castle Valley Sandstone, with 11WR-A-33 215172281 1.110.2325 0.93.66591.3 0.2721 0.90.71 1551.2 12.5 1564.010.11581.216.61581.216.6 99.2 11WR-A-38 149627653.7 9.9965 0.93.95641.8 0.2868 1.60.87 1625.7 22.4 1625.314.41624.716.11624.716.1 100.0 11WR-A-97 82 612772.3 9.9445 1.34.06001.8 0.2928 1.30.71 1655.6 18.5 1646.314.61634.423.51634.423.5 100.6 11WR-A-70 345804701.6 9.9313 0.43.31186.0 0.2385 6.01.00 1379.1 74.2 1483.846.81636.97.3 1636.97.3 92.9 11WR-A-28 484265571 2.49.86750.2 4.0800 1.00.29201.0 0.97 1651.5 14.8 1650.38.5 1648.84.5 1648.84.5 100.1 a reference stratigraphic section along Castle Creek. 11WR-A-63 124135729 0.99.86120.7 4.1956 2.20.30012.1 0.95 1691.7 31.7 1673.218.41650.013.51650.013.5 101.1 Paradox Formation 11WR-A-55 139169230 1.99.83660.9 4.1398 1.70.29531.4 0.84 1668.2 20.4 1662.213.61654.716.81654.716.8 100.4 11WR-A-26 203208488 1.19.83020.7 4.1060 2.30.29272.2 0.95 1655.2 31.9 1655.518.71655.912.81655.912.8 100.0 11WR-A-43 200126023 1.89.82260.4 4.0707 1.20.29001.1 0.93 1641.5 16.3 1648.49.9 1657.38.3 1657.38.3 99.6 11WR-A-99 106482531.1 9.6861 0.74.14022.4 0.2908 2.40.96 1645.8 34.2 1662.320.01683.212.31683.212.3 99.0 11WR-A-45 21091151 0.99.65310.6 4.1825 1.30.29281.2 0.90 1655.6 16.8 1670.610.51689.510.21689.510.2 99.1 11WR-A-35 1481177284.7 9.6191 1.04.28651.8 0.2990 1.50.84 1686.6 22.4 1690.814.81696.018.21696.018.2 99.8 11WR-A-65 366277041 2.69.55710.3 4.3941 1.50.30461.5 0.98 1713.9 21.91711.212.31707.95.1 1707.95.1 100.2 11WR-A-18 1571142762.0 9.4853 0.74.47061.6 0.3075 1.50.91 1728.6 22.5 1725.513.41721.712.11721.712.1 100.2 11WR-A-40 424108231 6.09.45060.9 3.5596 9.90.24409.9 1.00 1407.4 124.9 1540.678.81728.517.01728.517.0 91.4 11WR-A-29 192674612.4 9.4455 0.64.47251.9 0.3064 1.80.94 1722.9 27.3 1725.915.91729.511.71729.511.7 99.8 11WR-A-76 159748213.6 9.4224 0.64.50622.7 0.3079 2.70.98 1730.6 40.5 1732.122.71734.010.91734.010.9 99.9 Pennsylvanian Paradox evaporitic strata are mostly covered beneath surfi- 11WR-A-88 1901147882.7 9.3933 0.54.43562.8 0.3022 2.80.99 1702.1 41.3 1719.023.21739.68.3 1739.68.3 99.0 11WR-A-50 374514481.8 9.3417 0.24.67311.8 0.3166 1.80.99 1773.2 28.2 1762.415.31749.74.1 1749.74.1 100.6 11WR-A-75 411288462 2.99.20210.3 4.6566 1.70.31081.6 0.98 1744.6 25.1 1759.514.01777.25.7 1777.25.7 99.2 11WR-A-100 72 484333.4 9.0645 1.05.06492.0 0.3330 1.80.86 1852.8 28.5 1830.217.41804.718.81804.718.8 101.2 11WR-A-57 30 376661.5 8.6918 1.65.44592.3 0.3433 1.60.71 1902.5 27.1 1892.120.01880.729.61880.729.6 100.6 METHODS cial deposits of the valley floor in the northern extent of the valley, but limited 11WR-A-14 149106225 1.38.57970.5 5.5633 1.20.34621.0 0.90 1916.3 17.4 1910.410.01904.08.9 1904.08.9 100.3 11WR-A-8 170170483 0.68.54290.6 5.6456 3.80.34983.7 0.99 1933.6 62.2 1923.132.51911.710.21911.710.2 100.5 11WR-A-11 203354181.5 8.2232 0.75.06073.5 0.3018 3.50.98 1700.3 51.7 1829.529.91979.912.21979.912.2 92.9 11WR-A-41 29 30111 1.87.72062.6 6.9069 3.50.38682.4 0.68 2107.7 42.9 2099.531.42091.545.82091.545.8 100.4 11WR-A-16 72 908290.7 5.5689 0.611.2189 7.40.45317.3 1.00 2409.1 147.7 2541.568.82648.99.5 2648.99.5 94.8 11WR-A-34 214356711.3 5.4138 0.312.5708 1.50.49361.5 0.98 2586.2 31.7 2648.014.32695.65.0 2695.65.0 97.7 exposures are present in the northwesternmost part of the valley along the 11WR-A-78 49 186599 8.25.38510.8 13.32184.1 0.5203 4.00.98 2700.5 88.2 2702.738.52704.413.12704.413.1 99.9 11WR-A-92 154147345 1.45.34360.3 13.33141.6 0.5167 1.60.98 2685.0 34.4 2703.415.12717.25.3 2717.25.3 99.3 11WR-A-21 107201513 0.95.22190.3 14.26331.3 0.5402 1.20.96 2784.3 27.6 2767.412.02755.15.5 2755.15.5 100.6 11WR-A-47 208590586 1.85.16890.2 14.48752.5 0.5431 2.51.00 2796.5 56.7 2782.223.82771.84.1 2771.84.1 100.5 11WR-A-1 69 647542.2 5.0995 0.712.2560 2.40.45332.3 0.95 2409.9 45.7 2624.222.42794.012.02794.012.0 91.8 Data collection included geologic mapping of the NW end of Castle Valley base of cliffs directly south of the Castle Creek gorge and north of the creek 11WR-A-13 108175075 1.34.76770.2 16.63281.4 0.5751 1.40.99 2928.9 32.2 2913.913.32903.63.6 2903.63.6 100.5 11WR-A-54 40 884521.8 3.9716 0.522.4707 2.60.64732.5 0.98 3217.5 63.5 3204.324.83196.07.8 3196.07.8 100.4 at a scale of 1:10,000, measurement of stratigraphic sections at accessible in a wedge-shaped exposure that separates fluvial Cutler strata on the west 1Supplemental Table 1. U-Pb geochronologic analyses localities (details in Parr, 2012), and measurement of eolian foresets. Single from lower members of the Moenkopi Formation on the east (Figs. 5 and 6). of detrital zircons in Permian strata of Paradox Basin. measurements were taken for each dune bed set between bounding surfaces The Paradox Formation forms low mounds mantled by gypsum crusts south Please visit http://dx .doi.org/10 .1130/GES01174.S1 or the full-text article on www.gsapubs.org to view on a reference section along Castle Creek, but ten measurements were made of Castle Creek, but gypsum and shale are well exposed in a stream bank on Supplemental Table 1. per location elsewhere in the study area (Parr, 2012). Trough axes were mea- the north side of Castle Creek.

GEOSPHERE | Volume 11 | Number 5 Lawton et al. | White Rim–Castle Valley erg, Paradox Basin, Utah Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/11/5/1475/3335202/1475.pdf 1482 by guest on 01 October 2021 on 01 October 2021 by guest Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/11/5/1475/3335202/1475.pdf Research Paper Geologic Map of Northwestern Part Castle V 635000 635000 Triassic Jurassic 4279000 427 9500 4280000 4280500 4 281000 4 2 8 1 5 0 0 T Angular Unconformity Unconformity Angular Unconformity T rms North rmp Qa l Jkn Tr Jw c T T T T T 20 rms rmp rma rmt Tr Jw B rma do l ss ss c Surficial deposits Chinle Formation Moenkopi Formation T Wingate Sandstone Ross, 1998 (Jk?, Kayenta Formation of Doelling and Navajo and Kayenta Formation 2 1 2 C rma 18 T Sewemup Member Parriot Member Ali Baba Member Te rmt

of Dolostone unit at base salt weld growth strata east of sandstone members in Upper and lower

D nderfoot Member

Qa 63550 63550

Ali Baba Membe

P P P P P P P P P P P P P P P P P P P P P P P 17

o o o o o o o o o o o o o

o 14

rmt

) T

r r r r r r r r r r 0 r 0 rma c c c c c c Jkn c

u u u u u u u u u u u u u

15 Pccu

e e e e e e e e e

e 67

12 r

Jw Pccu

80 24 72 T Pennsylvanian s 7d 0 7b rmt 636000 636000 Pccl Pccl 21 56 67 18 26 24 70 27 22 7e 21 7a 30 25 33 33 33 ? 76 T 37 85 49 70 15 alley 33 rms 87 29 73 Pca 25 32 IP p Tr 48 36

70 Permian 7 43 38 37 43 c 36 9 dol 78 , Big Bend Quadrangle, Grand County 75 Qa Pca 73 40 68 Diapiric contac 5 23 Cutler Group 45 3 73 20 70 1 A′ IP p Pc a 41 25 IP p 72 8 25 Pccu 78 Pccl do l 23 37 60

636500 636500 Castle Va

dotted where concealed beneath younger unit Contact, dashed where located approximately’ dotted where concealed beneath younger unit dashed where located approximatel Fault (with subhorizontal slickensides; normal), C C C C C C C C C C C C C C C C 64 Synclinal hinge of growth monocline Anticline and anticlinal hinge of growth monocline Tr Strike and dip of beds overturned

t Castle

Undi Paradox Formatio 25 dol ?

mp 14 ace of salt weld 15 a a a a a a a a a a a a a a a a a 15

Lower eolianite membe Upper eolianite membe

s s s s Dolostone Caprock at Cutler-diapir contac s

Pca

Ca Ca Ca Ca

C 2

t 22 l l l l erentiated Cutler Formation arkose l

5 a e e e e e e e e

lley Sandstone e

st s s s s

ms V V V V V V V V

1000 m V Red interdune member

a a a a a a a a a a a a a

alley Tr

l l l l l l l l l l l l l l l l l

l l l l l l l l l l l l l l l l l l l l

l mt e e e e e e e e e e e e e e e e e

e ma

6 6

y y y y y y y y y y y y y y y y y y 37000 y 37000

C C Cr Cr Cr C Tr

r r r

Jk? ee Tr

e e e

k k k k y, B′ C′

D′ , Utah

4278500 4279000 4 2 7 9 5 0 0 4 2 8 0 000 4280500 4281000 4281500 t map. of Figure 7C spans south edge of in Figure 7. Oblique aerial view indicate locations of photo sites cated. Labels 7a, 7b, 7d, and 7e of cross sections of Figure 6 indi - western end of Castle Valley. Lines Figure 5. Geologic map of north -

GEOSPHERE | Volume 11 | Number 5 Lawton et al. | White Rim–Castle Valley erg, Paradox Basin, Utah 1483 Research Paper

TABLE 1. RECALCULATED MODAL POINT-COUNT DATA FOR CUTLER GROUP SANDSTONES, PARADOX BASIN QtFL QmFLt QmPK Biotite (%) (%) (%) (%) Sample1 Location2 Qt FL Qm FLtQmP K White Rim Sandstone 11WRA Shafer Trail 91 81 91 81 92 27 0 11WRB Hite 83 16 182162 83 4130 X87121 87 12 288310 SD 660661 614 Castle Valley (CV) Sandstone, upper 10CVW (DZ) CV anticline 88 12 088120 88 49 0 CVMS5-3 Castle Creek (Cr)9550935295140 CVMS5-36 Castle Creek 91 90 91 91 91 27 0 CV411 NE of anticline9190899191550 CV511 CV anticline 86 14 086140 86 59 0 CVMS4-18J CV anticline 96 40 95 41 96 14 0 CV811 Castle Valley 86 13 184133 86 4103 CVMS6-86 Castle Valley 80 20 079201 80 6140 CV611 South of Castle Cr 95 50 94 51 95 05 0 22 Castle Valley 95 50 94 51 95 05 0 X90100 89 10 19037 SD 550551 523 Castle Valley Sandstone, interdune member CVMS1-45J Castle Creek 86 13 185132 86 212<1 CVMS7-120 Castle Valley W78184 76 18 681415 1 X82163 81 16 484314 SD 642643 412 Castle Valley Sandstone, lower (bleached upper part) CVMS7-95 Castle Valley W9550945195230 CVMS5-5 South of Castle Cr 91 90 89 92 89 45<1 CVPO Castle Valley 89 11 087112 89 38 0 X928090829135 SD 330431 313 Castle Valley Sandstone, lower CVMS5-Base South of Castle Cr 84 16 083161 84 89<1 CVMS5-5 South of Castle Cr 79 20 176204 79 813<1 CVMS6-66 Castle Valley 66 33 165332 66 11 23 <1 12CV50 (DZ) Castle Creek 69 27 467276 71 920<1 12CV62 CV anticline 71 26 269264 73 11 16 0 CVMS23JA CV anticline 65 34 163343 65 15 20 <1 CVMS23JB CV anticline 67 32 166322 68 14 18 <1 CVMS7-30 Castle Valley W70282 69 28 371919 <1 CV911 CV anticline 73 24 372244 75 8171 10CVG (DZ) CV anticline 72 25 470264 73 9170 10CVR (DZ) CV anticline 69 29 269292 70 14 16 <1 X71272 70 27 3721117 SD 651651 634 (continued)

TABLE 1. RECALCULATED MODAL POINT-COUNT DATA FOR CUTLER GROUP SANDSTONES, PARADOX BASIN (continued) QtFL QmFLt QmPK Biotite (%) (%) (%) (%) Sample1 Location2 Qt FL Qm FLtQmP K Cutler Formation ﬂuvial facies Castleton 27.753 Castle Rock 61 37 261372 62 16 21 9 Castle Base Castle Rock 60 38 260382 61 17 21 4 11CVC01 (DZ) Castle Creek 54 45 153452 54 14 32 1 CVMS7-4.5 Castle Valley W50491 50 49 15022281 X56422 56 42 25717264 SD 561561 635 4 Note: Chert is included in Qt, Lt, and Qp grain categories. 1Sample number refers to Parr (2012), M.S. thesis, except samples 12CV-50 and -62. 2Locations: Castle Valley (CV)—west side of valley 700m south of Castle Creek; Castle Valley W—west side of valley 1.7 km south of Castle Creek; Castle Rock—northeast side of valley south of Castle Rock; CV anticline—crest of anticline north of Castle Creek; South of Castle Creek—west side of valley 300m south of Castle Creek. 3Approximate detrital-zircon locality 11CT01 at Castle Rock.

Undifferentiated Cutler Formation along Castle Creek (Fig. 8). Eolian strata are present in the subsurface of the salt-withdrawal minibasin, termed the Big Bend minibasin (Matthews et al., Permian red sandstone and conglomerate are exposed along cliff bases 2004, 2007; Banham and Mountney, 2013), between the Castle Valley and directly south of Castle Creek, where they abut Paradox exposures or surfi- Moab Valley salt walls, where 140 m of massive sandstone was penetrated cial deposits, and in an amphitheater-like bowl north of Castle Creek, where beneath the Moenkopi Formation in the Burkholder #1 well, 7 km southwest Cutler beds form a wedge of strata in which dip values decrease upsection of the outcrop (Fig. 4; Trudgill, 2011; Parr, 2012). The Castle Valley Sandstone but are everywhere steeper than those of overlying eolian strata. In the amphi does not crop out on the northeast flank of the salt wall but is present in the theater, Cutler strata strike north and northeast; individual beds steepen and subsurface north of the plunging nose of the structure, where the eolian sand- thin toward Paradox and Moenkopi strata on the northeast flank of the salt stone is ~50 m thick in the Grand River O and G #1 State well (Fig. 4; Trudgill, wall. Near-vertical conglomeratic beds are truncated beneath eolianite strata 2011; Parr, 2012). On the basis of the thickness in the O and G State well, the high on the northern slope of the amphitheater (Fig. 6, section C–C′), where Castle Valley Sandstone is inferred to be present but thin in the subsurface conglomeratic Cutler beds are bleached white below the contact. Cutler strata adjacent to the NE flank of the former salt wall beneath the Moenkopi Forma- thicken into northwest-elongate, salt-withdrawal minibasins on both flanks of tion (Fig. 6, sections B–B′, C–C′, and D–D′). The Castle Valley Sandstone is not the Castle Valley salt wall (Doelling and Ross, 1998; Doelling, 2002a, 2002b; exposed along the northeastern flank of the valley (Doelling and Ross, 1998; Kluth and DuChene, 2009; Trudgill, 2011). Doelling, 2002b), both because it was originally depositionally thin east of the nose of the salt wall (Fig. 4) and because it is truncated in the subsurface beneath the Moenkopi along the trend of the salt wall, as it is in outcrop on the Castle Valley Sandstone southwest side of the salt wall (Fig. 7C).

The Castle Valley Sandstone overlies undifferentiated Cutler strata on a discordant, sharp contact that ranges from only slightly angular on Castle Moenkopi Formation Creek (Fig. 7A) to strongly discordant at northernmost exposures. Bed sets of cross-bedded sandstone within the eolianite onlap Cutler strata along Castle The Lower Triassic Moenkopi Formation unconformably overlies the Castle Creek in the direction of the former salt wall (Fig. 7B). The eolianite crops Valley Sandstone on a discordant contact (Figs. 5, 6, and 7C). The top of the Castle out as cliffs on the southwestern flank of Castle Valley (Fig. 5) and thins to Valley Sandstone is an irregular surface marked by extensive desert varnish, pit- a pinch out beneath the Moenkopi Formation southeastward along the val- ting, and small sculpted ridges with amplitudes <1 m in the surface of the sand- ley wall (Fig. 7C; Doelling and Ross, 1998). The entire extent of the eolianite stone. The Moenkopi Formation is locally composed of four members defined in outcrop is just under 4 km long. The Castle Valley Sandstone is 158 m thick nearby eastern Colorado and at Castle Valley (Shoemaker and Newman, 1959).

Elevation (feet) Elevation (feet) Jkn Tr

Elevation (feet) 300 0 4000 5000 300 0 4000 5000 T rmp c 4000 300 0 5000 Jw D B CC T T rms rma T T T rmt rmt rmt Pccl T ′ . (B) Cross section B–B Pccl rma Pccl Pccu Pccu Pcwu Pcw l Qa T Pccu rmt Pc a Base over 12′ fault in T Qa Pcw rm draped ′ . (C) Cross section C–C Pca Pcu Pc a A–A′ T Pccu rmt T Pccl A–A′ rmp A–A′ A Pccu do l ′ . (D) Cross-section D–D T do l Tr Pccl ? c T Qa IP p ss do l Pca rmt Castle Cree k B–B′ 1 IP p ? T rma ss ss IP p do l Pcc Pccu 2 1 Pccl T T Pcc T T rma do l rma Pcc rms rmt ′ . C–C ′ Abrupt northward Pcc beneath do l truncation of ss Tr 2 T c rmt T Depth to IPp uncertain rmt T Tr rma Pccl m Pca T T rms rmp Pca Pca Pca T Tr rmp c ? T T rmp rmt B′ T D′ ? 300 0 4000 5000 D-D ' ′ rms 300 0 4000 5000 300 0 4000 5000 T Tr rma c A′ 300 0 4000 5000 6000

GEOSPHERE | Volume 11 | Number 5 Lawton et al. | White Rim–Castle Valley erg, Paradox Basin, Utah 1486 Research Paper

A B Pccu

Pccl

Pcci

Figure 7. Field photos and photomicrograph of Castle Valley Pca Sandstone. (A) Contact of Castle Valley Sandstone (Pccl) with underlying red arkosic strata of undifferentiated Cut- ler Formation (Pca) directly north of Castle Creek. Scale 1.5 m bar is 1.5 m high. (B) Stratigraphic relations in Castle Valley Pccl Sandstone directly north of Castle Creek. View north. Pccl— upper bleached part of lower eolianite member; Pcci—inter dune member; Pccu—upper eolianite member. Onlap of interdune member by upper member is demonstrated by thinning of lowermost set of upper member cross-beds, CDwhich pinches out updip of normal fault indicated by white arrow. Small foresets in upper left dip counter (black arrow) Jw to larger foresets in lower part of upper member. Interdune member is 7.5 m thick at right edge of photo. (C) Erosional Trc truncation of Castle Valley Sandstone beneath Moenkopi Formation along Porcupine Rim on southwestern flank of Trm Castle Valley. Base of Castle Valley Sandstone indicated by Trm white arrow. Pca—undifferentiated Cutler Formation arkose; Pccl—lower eolianite member of Castle Valley sandstone; Pcci Pcci—interdune member; Pccu—upper eolianite member; Trm—Moenkopi Formation; Trc—Chinle Formation; Jw— Wingate Sandstone. The inferred paleofluid contact in Pca the Castle Valley Sandstone, marked by contact between pink and white strata of lower eolianite unit, is truncated Pccu Pccu beneath the unconformity (orange arrow). Upper cliff of Porcupine Rim is 60 m high. (D) Fault in upper eolianite Pccl unit (Pccu) draped by basal Moenkopi beds (Trm). View north. Fault scarp is 3 m high. (E) Tar-saturated medium- to coarse-grained sandstone of grain-flow laminae alternate with fine-grained grain-fall and wind-ripple laminae, upper E F member of Castle Valley Sandstone. Hammer handle is 42 cm long. (F) Photomicrograph of lower eolianite member of Castle Valley Sandstone (sample CVSM23JA) near crest of Castle Valley anticline. Most grains are monocrystalline quartz; rounded grain in center is partially dissolved plagio clase; black interstitial material is tar; blue material is epoxy (pore space). Bimodal texture is evident.

0.5 mm

Measured Section, Petrographic Mean Ss Stratigraphic Eolian Foreset Castle Creek Sample Composition Unit Orientation (Table 1) 50 %Qt 100 Moenkopi Formation (Tenderfoot Member) Coarse grains and granules 0 %F 50 183 in deflation lag at top Angular unconformity CVMS5-36 Upper Castle Valley Sandstone Rose Diagram and Restored Foreset Dip Directions and Dip Values n = 42 Explanation Fluvial Environment Symbols

Pebbly sandstone CVMS5-3 Upper Castle Valley Horizontal lamination Sandstone Eolianite Trough cross-beds

Thickness (m) Scour and fill structure Figure 8. Measured section of Castle Burrows; trace fossils Valley Sandstone along Castle Creek. Dip tadpoles adjacent to section Rootlet traces indicate corrected foreset dip azi muths from measured section. Eolian Environment Symbols Stratigraphic variation in QtFL%Qt 100 (open dots) and QtFL%F (black Large-scale planar foresets dots) indicated by curves to right of dip tadpoles. Stereonets indicate all Trough foresets, generally dip directions and dip values (black less than one m in height dots), and resultant rose diagrams Climbing translatent strata for the lower and upper eolianite 10TPCV5T (DZ) units measured throughout the in horizontal or slightly Lower eolian bedset study area (see Fig. 10 for off-section onlaps interdune unit Interdune unit inclined beds localities). CVMS1-45J Conspicuous deflation lag White of granules and small CVMS6-66 pebbles at base of eolian vf m vc 10TPCV5R, 5G (DZ) f c Lower Castle Valley foresets Sandstone Eolianite Bounding surface Siltston e

Sandstone between bedsets Red 12 Petrographic sample site

CVMS5-5 DZ 12CV50 Detrital zircon sample site 12CV50 (DZ), CVMS5-Base Restored eolian foreset dip Scour Cutler Formation fluvial Lower Castle Valley Sandstone Resultant fluvial trough axis n = 20 trough facies, undifferentiated Rose Diagram and orientation limbs Restored Foreset Scour Dip Directions and Dip Values n = 15 11CVC01 (DZ) 0 m vc (~30 m below vff c 50 %Qt 100

Ss base section) Cgl.

Siltst . 0 %F 50

These members, which vary in thickness on the flanks of the Castle Valley salt and Buck, 2006). The weld continues upslope and is truncated at the base wall (Fig. 6; Lawton and Buck, 2006; Banham and Mountney, 2013), include of the Moenkopi Formation in the anticlinal hinge of the monocline (Fig. 6). the Tenderfoot, Ali Baba, Sewemup, and Parriot members (spelling of Parriot Cutler Formation beds west of the Paradox Formation strike north to northeast, Member by Shoemaker and Newman [1959] differs from the modern spelling steepening and thinning progressively to onlap the Paradox Formation and the of Parriott Mesa, adjacent to Castle Valley). The Moenkopi Formation ranges weld. All Moenkopi strata thin over the anticline and thicken eastward across from 135 to 375 m thick in exposures adjacent to Castle Valley (Lawton and the monoclinal flexure above the weld (Fig. 6). Buck, 2006) but probably exceeds 400 m along the Colorado River northeast High-angle faults of several trends displace the Cutler Formation and of Castle Valley where the basal contact lies in the subsurface (Shoemaker and Castle Valley Sandstone. Faults trending west and ENE (~060°) have apparent Newman, 1959). normal offsets of 15–50 m and displace former fluid contacts, marked by color Upper Triassic and Jurassic strata. The Upper Triassic Chinle Formation changes in the Castle Valley Sandstone (e.g., Gorenc and Chan, 2015) and overlies the Moenkopi throughout the Castle Valley region. The contact lies strata as young as Middle Jurassic on the Porcupine Rim (Fig. 5). These faults at the base of a coarse-grained angular sandstone on two hilltops north of have subhorizontal slickensides, are associated with minor antithetic strike- the amphitheater, where an angular unconformity at the base of the Chinle slip and reverse faults, and are present in the part of the map area where truncates 50 m of the Parriot Member of the Moenkopi Formation. The Chinle evaporite of the former salt wall pinches out northward, suggesting that they is overlain by thick-bedded eolian strata of the Jurassic Wingate Sandstone, accommodated differential NE-SW shortening where the mechanically weak which forms a steep escarpment, termed the Porcupine Rim, along the south- salt pinches out or thins to the point that it did not exert mechanical control on western flank of Castle Valley (Fig. 7C). Ledgy outcrops of the Jurassic Kayenta anticline development. Northwest-, NE-, and north-trending faults with less Formation form the rim of the escarpment (Figs. 5 and 6). than 5 m of displacement affect only the undifferentiated Cutler Formation and eolianite beds and terminate in the lowermost Moenkopi Formation. A conspicuous, north-trending normal fault that crosses the crest of the anti- Structural Geology cline offsets the Castle Valley Sandstone–Moenkopi contact 4 m and is draped by a wedge of strata in the lowermost Moenkopi, indicating fault movement The major structural feature of the NW end of the Castle Valley is an open ended near the beginning of Moenkopi deposition (Fig. 7D; Banham and northwest-plunging anticline that forms the continuation of the salt wall be- Mountney, 2013). yond the inferred surface extent of the Paradox Formation. The anticline, best In addition to local draping of faults by basal Moenkopi strata, thickness seen on cross section A–A′ (Fig. 6), is expressed in the Castle Valley Sandstone trends and stratal geometries of Permian and Early Triassic strata demonstrate and Moenkopi Formation north of Castle Creek (Fig. 5) and plunges northwest- syndepositional growth of the folds in the study area. Upturn and onlap of un- ward to terminate abruptly at the Colorado River; it has little structural expres- differentiated Cutler beds onto the Paradox Formation and weld indicate that sion in the Chinle Formation, which thins southeastward onto the anticlinal the beds were deposited directly on exposed Paradox evaporite and subse- nose by onlap onto the Moenkopi Formation (e.g., Shoemaker and Newman, quently folded by continued diapirism to form halokinetic sequences adjacent 1959; Matthews et al., 2004, 2007). North of Castle Creek, a monocline with to the diapir (sensu Giles and Lawton, 2002; Rowan et al., 2003; Giles and ~150 m of structural relief in the middle part of the Moenkopi Formation trends Rowan, 2012). Thinning of eolianite and Moenkopi beds across the crest of northward, obliquely to the crest of the anticline, and decreases in amplitude the northwest-trending anticline and thickening of the Moenkopi Formation along its northward plunge to a termination at the Colorado River. The mono- eastward across the monocline indicate that both the anticline and the monocline creates only 30 m of structural relief on the unconformity at the base of cline grew during deposition of the Castle Valley Sandstone and Moenkopi the Chinle Formation, and 49 m of the Parriot Member is removed beneath Formation (Fig. 6; Lawton and Buck, 2006; Banham and Mountney, 2013). The the unconformity across the monocline (Fig. 6, D–D′), relations which indicate growth of these structures was largely complete by deposition of the lower that most structural development of the monocline took place prior to Chinle part of the Chinle Formation. A restoration of cross section D–D′ from the Late deposition. Triassic back through deposition of the eolianite indicates that the Paradox North of Castle Creek, the Paradox Formation occupies a northward-taper- Formation was exposed on the crest of the monocline for much of the growth ing exposure that separates fluvial Cutler strata on the west from the Tender- history of the anticline (Fig. 9). Although it is not clear that the Paradox For- foot Member of the Moenkopi Formation on the east. The Paradox Formation mation was always exposed during deposition of the Castle Valley Sandstone, thins and pinches out northward, merging into a fault-like surface that sepa- sedimentological and compositional features described below suggest that rates Cutler from Moenkopi strata, all of which face away from the surface. the diapir was exposed during at least some parts of the depositional history This surface represents a salt weld (e.g., Jackson and Cramez, 1989) formerly of the eolianite and that the diapir had topographic relief that influenced dis- occupied by diapiric evaporite between the Cutler and Moenkopi beds (Lawton tribution of eolian sand.

Base Sewemup Flat Cross section D-D′ C Trc D Trmp Trc D′ Trma 5000 Trmt Trmp Pccu Trmt Pcwl Trms Pcc Pca Trmt Trma Pccl Pca IPp Pccu 4000 Trmt Pca Pca dol Pcc Elevation (feet) Pccl IPp D Base Ali Baba Flat dol Figure 9. Restoration of cross-section 3000 Trmt D–D′ of Figure 6 from deposition of Pccu Pcc Chinle Formation to beginning of depo Pca sition of Castle Valley Sandstone. Upper left: Cross section D–D′ (see Fig- A Base Chinle Flat Pccl IPp ure 5 for location). (A) Cross section Trmp Trms D–D′ restored to onset of deposition of Chinle Formation. (B) Cross section Pca D–D′ restored to onset of deposition of Parriott Member of Moenkopi Forma- Trma Trmt tion. (C) Cross section D–D′ restored to Pccu Base Moenkopi (Tenderfoot) Flat onset of deposition of Sewemup Mem- Trmt E ber of Moenkopi Formation. (D) Cross Pcc Pcc section D–D′ restored to onset of depo- Pca Pccu Pca Pccl IPp sition of Ali Baba Member of Moenkopi Pca Pccl IPp Formation. (E) Cross section D–D′ restored to onset of deposition of Tender- Pca foot Member of Moenkopi Formation. (F) Cross section D–D′ restored to onset of deposition of upper eolianite mem- B Base Parriott Flat ber of Castle Valley Sandstone. Trms F Base Upper Castle Valley Sandstone Flat Trma Pccl Pcc Trmt Pca Pccu Trmt Pca IPp Pcc Pccl Pca IPp Pca

SEDIMENTOLOGY OF PERMIAN UNITS bodies 2–4 m thick with scour fills and pebble-filled troughs near bed bases. Pebbly trough cross-beds decrease in height from 35 to 10 cm upsection The undifferentiated Cutler Formation and Castle Valley Sandstone consti- through channel bodies. Trough cross-beds are typically overlain by hori- tute the exposed components of the Permian depositional system in Castle zontal, discontinuous, normally graded laminae 5–15 mm thick, locally with Valley. The undifferentiated Cutler Formation consists of reddish-brown, an- pebbles dispersed on the laminae. Horizontally laminated sandstone is in- gular, medium- to very coarse-grained, poorly sorted sandstone and pebbly terpreted as deposits of antidunes by unconfined flow in the shallow parts sandstone. Sandstone beds consist of upward-fining, broadly channel-form of channel systems (e.g., Blair and McPherson, 1994). Burrows and rootlet

traces occupy the upper parts of some channel bodies. Pebbles and cobbles eolianite (Fig. 7E). Some large-scale bed sets in the upper eolianite are com- are angular to rounded, as much 28 cm in diameter, and consist of granite, plex and contain small-scale foresets with dip directions opposite to those of biotite schist, gneiss, and quartz. A single paleocurrent site consisting of the large foresets (Fig. 7B), indicating that smaller bed forms climbed the large- trough cross-beds on Castle Creek near meter 20 of the measured reference scale dunes. Uncommon low-angle laminae of climbing translatent strata are section yielded a NNW (355°) paleocurrent direction (Fig. 8). The resultant present in the upper member (Fig. 8). Slumping of slip-face bed sets was not direction is similar to consistent northwest-directed paleocurrent indicators observed in either eolianite member. reported from approximately correlative Cutler red beds elsewhere in Castle The interdune member overlies the lower eolianite on a sharp contact, and Valley on the SW flank of the salt wall and in the upper part of the undifferen- consists of reddish-brown medium- to very coarse-grained pebbly sandstone tiated Cutler Formation in the Onion Creek drainage, 10 km to the northeast with discontinuous, weakly defined, inversely graded horizontal laminae and (Fig. 4; Buller, 2009), as well as mean paleocurrent directions reported from shallow pebble-filled scours. The lower contact locally consists of a surface the upper part of the Cutler Formation in the same area (Venus et al., 2015). with as much as 50 cm of relief filled locally by a pebble lag and elsewhere by The northwest-oriented sediment-dispersal directions in the upper part of the separate pebble lenses in fine-grained sandstone. Pebbles consist of angular Cutler section indicate fluvial dispersal parallel to the Castle Valley salt wall. to subrounded granules and pebbles of granite, quartz pebbles as much as 2 Northwestward sediment transport parallel to the elongate minibasins has cm in diameter, and angular clasts of medium-gray dolostone to 6 cm long. also been documented in the overlying Moenkopi Formation (Banham and The dolostone clasts resemble dolostone of blocks in diapiric Paradox evapo- Mountney, 2013, 2014). Deposition of the undifferentiated Cutler section took rite exposed elsewhere in Castle Valley and also resemble dolostone caprock place in pebbly braided channel systems in the salt-withdrawal minibasins on that flanks the salt wall (Figs. 5 and 6; Shock, 2012). The interdune member is both sides of the wall. 7.5 m thick at creek level and thins up dip to a pinch out but persists as an ero- The Castle Valley Sandstone consists of two sandstone units with large-scale sion surface with discontinuous pebble lags between the eolianite members to cross-stratification separated by a laterally continuous, lightreddish-brown the northern extent of exposure. sandstone interval containing pebble lags and scattered pebbles (Fig. 8). Sedimentary structures of the Castle Valley Sandstone indicate deposition These stratigraphic units, continuous throughout exposures of the Castle Val- by large dunes preserved adjacent to the Castle Valley salt wall. Coarse-grained ley Sandstone, are termed the lower eolianite, interdune, and upper eolianite inversely and normally graded sandstone laminae with scoured bases in large members. Sedimentologic features of the lower and upper eolianite members planar foresets are interpreted as sand-flow or grain-flow laminae (e.g., Hunter, are similar and are described together. The lower eolianite is 40 m thick along 1977; Mountney, 2006), and intervening thin laminae are interpreted as grain- Castle Creek, where it overlies the undifferentiated Cutler Formation on a sharp fall deposits and wind-ripple laminae (Hunter, 1977; Fryberger et al., 1988), contact (Fig. 7A) that truncates syndepositional normal faults with centime- which together constitute slip-face deposits (e.g., Mountney, 2006). Marked ters of displacement in the underlying arkose. Northward and up dip from the cm-scale cyclicity in slip-face deposits containing successions of climbing measured section, the contact is gradational and interfingering, with apparent translatent strata, grain-fall and sand-flow laminae, like those in the Castle Val- reworking of eolian sandstone into pebbly facies. The lower eolianite consists ley Sandstone (Fig. 7E), have been interpreted as a consequence of diurnal on- of moderately sorted, light reddish-brown sandstone with planar cross-beds in shore sea breezes in coastal dune fields of the Texas Gulf Coast (Hunter, 1977) tabular sets 2.5–12 m thick in its lower part. The uppermost 5 m of the lower and thus might record very rapid accumulation of Permian dune sediment, an member is composed of trough-form foresets 0.25–0.5 m thick and is white inference supported by detrital-zircon data described below. Smaller wedge to yellow along the entire outcrop belt, in contrast with the uniform light sets represent subordinate transverse or barchanoid dunes superimposed on reddish-brown color of the rest of the member. The upper eolianite is 108 m the larger dunes, with opposing dips possibly resulting from seasonal changes thick along Castle Creek and consists of well-sorted white to tan sandstone in wind directions. Broadly trough-shaped foresets at the top of the lower eoli- with dominant planar cross-beds in tabular to broadly wedge-shaped sets anite member are interpreted as deposits of small barchanoid dunes deposited 1–22 m thick. Subordinate trough cross-beds generally less than 1 m thick are prior to cessation of lower member deposition. present in the lower part of the member (Fig. 8). At Castle Creek, the lower con- The interdune member represents fluvial sheet-flood deposits. Uncon- tact of the upper member is unconformable, indicated by thinning and onlap fined, supercritical flow created antidune deposits recorded by discontinu- of the basal dune bed set onto the interdune member (Fig. 7B). The large-scale ous inversely graded sandstone layers with scattered pebbles (e.g., Blair and foresets of both eolianite members are composed of alternating lamina sets of McPherson, 1994). The flow reworked the upper part of the lower eolianite very fine to fine-grained and medium- to coarse-grained sandstone. Coarser member and steeply-dipping undifferentiated Cutler beds, the source of many laminae are 3–20 mm thick and laterally continuous to broadly lenticular on of the pebbles, and also transported pebbles from resistant dolomite blocks bedding-parallel surfaces, and have scoured bases. Fine-grained laminae are and caprock of the diapir, which was exposed during deposition of the inter- ~1 mm thick and form co-sets 5–10 cm thick between the coarser laminae to dune member (e.g., Fig. 9F). The interdune member thins up dip toward the yield a marked cyclicity in the large-scale cross-beds, especially in the upper diapir as a result of decreased accommodation toward the diapir crest.

Foreset orientations in the Castle Valley Sandstone vary but indicate pre- 635500 6 36000 636500 dominant transport directions to the southwest and southeast (Figs. 8 and 10). The lower eolianite member, in which most of the paleocurrents were measured on the Castle Creek section, is dominated by southwest foreset dip di- 0 0 1000 m 0

rections, although there are a few large foresets oriented to the northeast and 28100

4 Pccl 428100 southeast (Fig. 8). The dominant southwest transport direction indicates that the sand was deposited on the lee side of the salt wall. Transport directions in Qa the upper eolianite member were to the southwest and southeast, perpendic- Trm ular to and parallel to the salt wall, respectively. The variability of wind direc- Pccu tions indicated by foreset orientations in both units suggests that the Castle Valley Sandstone records deposits of a draa that consisted of several types of superposed dunes, possibly star, linear, and transverse dunes, in a dune field Pca adjacent to the salt wall. It thus constitutes the exposed part of an irregularly

distributed dune field that was preserved against the flanks of salt walls and 4280500 4280500 dol in intervening minibasins (Fig. 4; e.g., Dubiel et al., 1996; Trudgill, 2011; Parr, IPpCreek 2012; Rasmussen, 2014). Castle Qa Pccu SANDSTONE PETROGRAPHY IPp 0

Sandstone composition and texture change upsection from the Cutler flu- 00 0 0 8 2 4 vial facies into the eolian facies of the Castle Valley Sandstone and likewise 428000 change upsection through the Castle Valley Sandstone itself. The upper mem- Pca ber of the Castle Valley Sandstone is compositionally similar to the White Rim Pccl Sandstone to the southwest. N The undifferentiated Cutler Formation consists of poorly to moderately sorted, fine- to very coarse-grained angular to subangular sandstones with Trc pervasive but unevenly distributed hematite grain rims locally as much as 0 0 0 10 mm thick. Coarsely crystalline, granular to rhombohedral calcite forms small 0 95 95 7 patches and locally forms pervasive pore-filling cement. The fluvial strata con- 7 42 42 stitute compositional arkoses with an average composition of Qt56F42L2 (n = 4; Trm Table 1). Potassium feldspar, including abundant microcline, comprises ~60% of the feldspar population, and subordinate plagioclase ranges from unaltered to partly dissolved and replaced by calcite (Fig. 7F). Biotite and muscovite are common, reaching a maximum of 12% of detrital grains; biotite constitutes about three-fourths of the mica. Metamorphic lithic fragments, which include Pca

foliated quartz-muscovite schistose fragments and a single observed meta Jkn 0 rhyolite grain, are uncommon in the samples studied. Granitic rocks domi- 279000 427900 nated the source area of the fluvial sandstones. 4 The Castle Valley Sandstone ranges from compositional arkose to subar- Jw kose; mean quartz content increases upsection (Figs. 8 and 11). Nearly ubiqui tous bimodal sandstone textures result from laminae of alternating, coarse, 635500 6 36000 636500 subrounded to rounded grains and fine angular to rounded grains. Grains in Figure 10. Map of wind directions in Castle Valley Sandstone indicated by restored eolian foreset coarse-grained laminae range from 0.4 to 2.5 mm in diameter; those in fine dip directions (dip tadpoles) measured throughout the field area. Locations other than Castle laminae are well sorted and consistent at 0.1–0.3 mm in diameter. In the red Creek section are averages of ten foreset measurements (Parr, 2012). Data are revised from Parr (2012), except tadpoles along Castle Creek, which are taken from Figure 8 as space permits. A part of the lower eolianite member, coarse laminae contain grains of rounded single fluvial paleocurrent locality in the upper part of the undifferentiated Cutler Formation is monocrystalline quartz, subrounded to rounded potassium feldspar, includ- indicated by arrow north of Castle Creek.

Qt A B Mean White Rim Sandstone Craton Qt (n = 76; Steele-Mallory, 1982) Interior White Rim Sandstone (n = 2) Upper Castle Valley Ss (n = 9) Figure 11. QtFL plot for Cutler Group sandstones. See Transitional Castle Valley Ss Interdune Table 1 for point-count data. (A) Individual sample point Continental (n = 2) counts. (B) Mean modal compositions and 1σ standard de- viation polygons for data of triangle A. Stratigraphic units White lower Castle Valley Ss Recycled are arranged in ascending stratigraphic order in explanation. Basement orogenic (n = 3) Uplift Recycled Red Lower Castle Valley Ss orogenic Qt = 40% (n = 11) F Dissected Arc L Cutler fluvial facies (n = 4) Qt = 40% F L

ing abundant microcline, and less common plagioclase. Potassium feldspar specks of tar are present in all samples of the white sandstones, particularly in is unaltered, but plagioclase is almost universally replaced by fine-grained coarse-grained laminae, and in some samples degraded oil occupies one-third clay of moderate birefringence, microcrystalline white mica or mixtures of of the porosity, including secondary pores after plagioclase. The dominant hematite and calcite, or it is partially dissolved. Even reasonably fresh grains cement constitutes thin discontinuous rims of high-birefringence clay, proba- are partly altered to microcrystalline white mica. Plagioclase alteration results bly illite, and carbonate cement forms poikilotopic nodules in some samples. in some uncertainty as to the original plagioclase content of the sandstones Hematite rims are absent. The fine-grained fraction of both lower and upper because some secondary pores contain no evidence of their original detrital eolianite members is somewhat richer in quartz than the coarse-grained frac- occupant. Uncommon globules of tar occupy some of the secondary pores tion; primary quartz overgrowths, developed in situ, are not present in either (Fig. 7F). Some quartz and feldspar crystals constitute polycrystalline granitic of the eolianite members. rock fragments with interlocking granular texture. Muscovite and biotite are The interdune member consists of angular to rounded, moderately sorted locally common as fine detrital grains at the boundaries between coarse and sandstone with rounded grains to 0.5 mm in diameter, although most grains fine layers. Uncommon rounded hornblende is present. Reddish-brown sand- are subangular to rounded in the range 0.1–0.2 mm in diameter. The grain stones of the lower eolianite member have thin rims of hematite cement that rounding and range of grain sizes of the unit are thus similar to those of the are not present in the upper white part of the member or the upper member. lower eolianite member, but the sandstones lack the segregated bimodal tex-

The average composition of the lower eolianite member is Qt71F27L2 (n = 11; tural aspect characteristic of the eolianite. Hematite rims range from light to Table 1); potassium feldspar, including microcline, averages about two-thirds moderate, and are not present on all grains, suggesting recycling of grains of the feldspar content. Only one sample (CV911; Table 1) contains apprecia- from previously oxidized sandstones. The average composition of two sam-

ble metamorphic lithic fragments (3%) consisting of schistose and polygonal ples is Qt82F16L3. Plagioclase constitutes somewhat less than one-third of the quartz-mica fragments. feldspar. Lithic grains include carbonate lithic grains composed of rhombic The upper white part of the lower eolianite member and the upper eolianite dolomite crystals, which make up 3% of one sample (CVMS7-120). Biotite and member are compositionally and texturally indistinguishable, are enriched in muscovite are present in both samples. The texture and composition are read- quartz relative to the lower member, tend to have more rounded grains, and ily explained by incorporation of detrital components derived from subjacent have more samples that lack coarse-grained laminae. Average composition of eolianite, upturned Cutler beds adjacent to the diapir, and resistant carbonate

the white upper part of the lower eolianite is Qt92F8L0 (n = 3) and of the upper lithologies in and possibly adjacent to the diapir.

eolianite is Qt90F10L0 (n = 10). Plagioclase averages only 3% of the QtFL content White Rim Sandstone samples of the greater erg to the southwest are simi- of both units; in some samples, all plagioclase was inferred from secondary lar in texture and composition to the white parts of the Castle Valley Sandstone. pores. Rounded grains of monocrystalline quartz with abraded, discontinuous A sample collected near the base of the Shafer Trail in Canyonlands National quartz overgrowths, which indicate recycling of some quartz grains from a sedi Park (Fig. 3; 11WRA) lacks coarse grains, whereas a sample from Hite on Lake mentary source, are present and even common in some samples. Both white Powell (11WRB) contains laminae with scattered coarse grains. As with the intervals are distinguished by the presence of rare chert grains, a sedimentary Castle Valley Sandstone, the grains are better rounded in the coarser laminae lithic grain type not observed in the undifferentiated Cutler or lower eolianite and as much as 0.75 mm in diameter. The two White Rim samples have an aver

samples. Biotite is typically absent but constitutes 3% of detrital grains in one age composition of Qt87F12L1 (Table 1), but they differ substantially in feldspar sample (CV811). Porosity is high, as much as 25%, in both units. Globules and composition: The Hite sample has 16% feldspar and the Shafer Trail sample

has only 8% feldspar. The alkali feldspar is exclusively orthoclase; microcline near Hite, Utah. Samples were collected from the undifferentiated Cutler For- is absent. Plagioclase is present but subordinate to orthoclase, and mica is ab- mation ~56 m beneath the unconformity with the Moenkopi Formation on sent. Our counts are somewhat more feldspathic than the mean composition, the northeast side of Castle Valley (Fig. 4; sample 11CT01) and north of Castle

Qt96F2L3, of the White Rim Sandstone between the Green and Colorado rivers Creek ~30 m stratigraphically beneath the base of the Castle Creek measured in Canyonlands National Park (Fig. 10, Table 1; n = 76; Steele-Mallory, 1982). section (sample 11CVC01). Castle Valley Sandstone samples were collected on In summary, sandstone composition changes upsection through the Castle and near the Castle Creek measured section (Fig. 8), and White Rim Sandstone Valley Sandstone (Table 1). Total quartz decreases from an average of 56% in samples were collected at South Fork Wash near the base of the Shafer Trail the fluvial facies to 92% and 90% in the upper white part of the lower eolianite in Canyonlands National Park and from a road cut on Utah Highway 95 on and upper eolianite, respectively. Total feldspar decreases in concert with the the north side of the Colorado River (Lake Powell) opposite the site of the for- upsection increase in quartz, from 42% in the fluvial facies to 8% and 10% mer Hite Marina, 1.8 km east of the confluence of the Colorado and Dirty Devil in the white eolianite intervals (Fig. 8). Common transported overgrowths on rivers (Fig. 3). quartz grains and uncommon chert in the white intervals provide evidence for sedimentary rocks in the source area; chert and transported overgrowths were not observed in the fluvial facies or the lower eolianite member. The interdune Zircon Age Populations member is somewhat more feldspathic than the underlying white part of the upper eolianite and so breaks the monotonic trend to higher quartz content Seven zircon grain-age populations were defined on the basis of all U-Pb de- with height in the section. It also contains the only detrital carbonate grains trital grain ages measured in the sample set (Fig. 12A; n = 729 individual grain observed in the sandstone suite. As noted, the composition and texture of the analyses; N = eight sandstone samples; Supplemental Table 1 [see footnote interdune unit likely resulted from recycling of resistant dolomitic clasts and 1]). The discordance and error filters resulted in the rejection of 17 analyses caprock from the diapir and fluvial Cutler strata upturned adjacent to the diapir, (of 746 total); the rejected grains, of which three are Archean, one is 1550 Ma, realistic possibilities indicated by the structural restoration (Fig. 9F). five are Grenville, and eight are Paleozoic, are indicated in strikethrough text The stratigraphic trends toward increased compositional and textural main Supplemental Table 1 (see footnote 1). Detrital-zircon grain ages range from turity can be explained by appealing to two possible, but mutually exclusive, ca. 3339 Ma to ca. 299 Ma; age populations consist of grain clusters on the mechanisms. Upsection loss of feldspar and concomitant enrichment in quartz probability distribution plots separated by age gaps and, except for Population could have resulted from feldspar destruction in a single sand population B, defined below, contain one or more age peaks (Fig. 12A).Table 2 is a com- during transport-related abrasion, perhaps aided by chemical weathering of pilation of grain-population ages, age peaks, numbers of zircon grains in each feldspar. The other possibility is that locally derived arkosic sands were mixed population and inferred sources for the grains. with and diluted by a sand population transported to the basin from another source by eolian processes. There is abundant evidence for postdepositional loss of pristine plagioclase, and analogous chemical weathering could have Population A (~3539–2548 Ma) affected the grain populations during transport. On the other hand, the presence of a sedimentary source for grains in the upper part of the Castle Valley Archean zircons constitute 4% of grains (n = 32), with a wide range of ages Sandstone, indicated by transported quartz overgrowths and chert grains, cor- with overlapping 1s age uncertainties. Archean zircons are absent from the roborates the second hypothesis of dilution of local sand populations by eolian fluvial facies of the Cutler Formation, being restricted to the Castle Valley Sand- sand input. Increased rounding of grains in younger eolianite strata resulting stone (5% of all analyses) and the White Rim Sandstone (9%). from more extensive transport-related abrasion presumably could have taken place in either scenario. Detrital zircons from the various units provide a basis for selecting between Population B (~2456–2008 Ma) the two hypotheses. Older Paleoproterozoic zircons are uncommon and represent only 2% of the total grain population (n = 14). This is a population of dispersed grain ages DETRITAL ZIRCONS that do not all overlap at 1s uncertainty; therefore, the population does not contain any significant age peaks. Grains of this population are present in all U-Pb detrital-zircon geochronology of samples from the Cutler Group indi- samples of the Castle Valley Sandstone and the White Rim Sandstone (Figs. cates significant differences in detrital-zircon content among the fluvial facies 12B, 12D, and 13) but are absent from the Cutler fluvial facies (Figs. 12C and of the undifferentiated Cutler Formation, the Castle Valley Sandstone, and the 13). Basement rocks of this age (2.3–1.8 Ga) are present in the Wopmay orogen White Rim Sandstone of the greater erg in Canyonlands National Park and of northwestern Laurentia and the Trans-Hudson orogen of central Laurentia

G FEDBC AAG F E D C B 1440 200 AB1441 All Cutler samples Castle Valley Sandstone (n = 729; N = 8) 50 (n = 357; N = 4) 419

150 40

30 1719 100 328 1042 624 1723 424 20

50 2737 Figure 12. Probability density plots and 1041 Relative Probabilit 10 grain-age histograms of Cutler Group 328 624 sandstones. Detrital-zircon populations in- 2697 dicated across top of plots and highlighted by vertical color bars. N is number of sam- 0 0 ples; n is number of individual grain analy- 425 ses. All histogram bins are 50 m.y. (A) Age CDCutler fluvial facies White Rim Sandstone distribution of all zircon grain analyses of Number 140 1441 16 this study. (B) Age distribution of Castle (n = 198; N = 2) (n = 174; N = 2) Valley Sandstone samples. (C) Age distribution of undifferentiated Cutler Forma- 120 14

y tion samples. (D) Age distribution of White 1134 1649 Rim Sandstone samples. 100 12 1038

10 80 606

8 60 1788 1724 6 2750 40 4

20 2

0 0 0500 1000 1500 2000 2500 3000 3500 4000 0500 1000 1500 2000 2500 3000 3500 4000 Age (Ma) Age (Ma)

(Dickinson and Gehrels, 2009; Gehrels and Pecha, 2014). Basement rocks of Population C (~1991–1599 Ma) this approximate age range (2.25–2.05 Ga) are also present in the Maroni- Itacaiunas basement province on the northeastern flank of the Amazonian Late Paleoproterozoic zircons of population C constitute abundant grains craton (Cordani et al., 2009; Cardona et al., 2010). Detrital-zircon grains rang- in the analyzed samples and include 22% of all grain analyses (n = 161) with ing ~2.25–2.00 Ga, of inferred Gondwanan derivation, are present in Paleozoic dominant peaks near 1750 Ma, 1723 Ma, 1666 Ma, and 1650 Ma. This pop- sedimentary rocks of the Suwannee terrane of Florida, southeastern Alabama, ulation is of roughly equal abundance in all samples, ranging from 17% to and southern Georgia (Mueller et al., 2014). 27% of grains in individual samples; it is somewhat more abundant in White

TABLE 2. U-PB DETRITAL-ZIRCON AGE POPULATIONS IN CASTLE VALLEY EOLIANITE, CUTLER GROUP, AND WHITE RIM SANDSTONE Age range Age peaks Age population (Ma)1 (Ma2)n3 % of Total4 Possible ultimate source References (1) Wyoming craton; ~3539–2548 Jessup et al. (2006); Dickinson and Gehrels (2009); A Ca. 2697 32 4 (2) Paleoproterozoic quartzite units of Uncompahgre uplift (Archean) Jonesetal. (2009) and San Juan dome (1) Wopmay orogen of NW Laurentia; ~2456–2008 (2) Paleoproterozoic quartzite units of Uncompahgre uplift Hill and Bickford (2001); Jessup et al. (2006); Cordani et al. B 14 2 (Early Paleoproterozoic) and San Juan dome; (2009); Jones et al. (2009); Cardona et al. (2010) (3) Maroni-Itacaiunas basement province of Brazilian craton (1) Yavapai province of SW Laurentia; (2) metamorphosed volcanic and plutonic rocks of Ca. 1842, 1800, Bickford et al. (1989); Jessup et al. (2006); Gonzales and ~1991–1599 Uncompahgre uplift (Gunnison area and Black Canyon) C 1783, 1750, 1723, 161 22 Van Schmus (2007); Dickinson and Gehrels (2009); (Late Paleoproterozoic) and Needle Mountains of San Juan dome; 1666, 1650 Jones et al. (2009) (3) Paleoproterozoic quartzite units of Uncompahgre uplift and San Juan dome (1) 1.4 Ga granite-rhyolite suite of Laurentia; (2) 1.44–1.35 Ga plutons in Uncompahgre uplift Bickford and Cudzilo (1975); Tucker and Gower (1984); ~1581–1302 Ca. 1575, (Unaweep and Black canyons) and San Juan dome Anderson (1989); Tewksbury (1989); Wasteneys et al. D 267 37 (Early Mesoproterozoic) 1550, 1441 (Needle Mountains); (1997); Jessup et al. (2006); Gonzales and Van Schmus (3) Sveconorwegian orogen; (2007); Bingen and Solli (2009) (4) Pinware terrane, SE Labrador ~1288–900 Ca. 1268, 1179, E (Late Mesoproterozoic– 126 17 Grenville orogen of eastern United States Dickinson and Gehrels (2003) 1135, 1041 Early Neoproterozoic) Iapetan synrift volcanics of eastern and southern ~734–499 Ca. 643, 624, Laurentia (~765–530 Ma); Pan-African and peri- F (Late Neoproterozoic– 57 8 Thomas (2011, 2014); Mueller et al. (2014) 608, 569, 536 Gondwanan terranes of Appalachian orogen and Cambrian) south of Ouachita orogen Greater Appalachian orogen: Taconic orogen ~491–283 Ca. 455, 424, G 74 10 (~490–440 Ma); Acadian orogen (~420–350 Ma); Dickinson and Gehrels (2003); Thomas (2011) (Paleozoic) 380, 328 Alleghanian orogen (~330–270 Ma) 1Age ranges are cohorts of ages with overlapping 2σ uncertainties separated by age gaps. 2Peak ages picked using Age Pick algorithm of Gehrels (https://docs.google.com/document/d/1MYwm8GcdYFOsfNV62B6PULb_-g2r1AS3vmm4gHMOFxg/preview). Listed peaks (plain text) based on nine or more grains, major peaks (bold text) on 39 or more grains. 3n= number of analyses in age population. 4Total = total number of analyses = 729.

Rim samples (26% and 27%) than in fluvial and eolian Cutler samples. Despite metavolcanic and granitic rocks now exposed in Unaweep and Black Canyons the apparent equal grain abundance in all samples, the range of grain ages in (Fig. 1) that range in age from 1755 Ma to 1670 Ma (Bickford et al., 1989; Jessup the fluvial Cutler samples is significantly narrower than in the White Rim and et al., 2006). Basement rocks of this age are also present to the southeast in Castle Valley Sandstone samples, being restricted to ~1790–1689 Ma, with a the San Juan dome, where they include metavolcanic and metaplutonic rocks mode in the 50 m.y. range of 1750–1700 Ma (Fig. 12C). The distinctive, more in the Needle Mountains, including the Irving Formation (1810–1780 Ma) and restricted age range of ~1790–1689 Ma is designated subpopulation C′. Twilight Gneiss (1772–1754 Ma; both ages U-Pb zircon upper intercept; Gonza- Grains of population C could have been derived from basement of the les and Van Schmus, 2007) and granite plutons that intrude them (Tewksbury, Yavapai-Mazatzal province in southwestern Laurentia, and the Trans-Hudson, 1989), including the Tenmile Granite (1716 ± 10 Ma) and the Bakers Bridge Central Plains, and Penokean provinces in the interior of Laurentia (see Dick- Granite (1698 ± 4 Ma; both ages U-Pb zircon upper intercept; Gonzales and inson and Gehrels, 2009, for a synthesis of basement-age provinces of Lau- Van Schmus, 2007). Detrital zircons in Paleoproterozoic quartzite units, the rentia). In the Early Permian, nearby sources of these grains were present in Cebolla Creek Quartzite of the Black Canyon and Uncompahgre Formation of exposed basement rocks of the Uncompahgre uplift. These sources include the Needle Mountains, are dominated by zircons in this age range (94%; n =

Population D (~1581–1302 Ma) 328 Diamond Creek Ss (06UT01; n = 91) 1068 1701

422 Early Mesoproterozoic grain ages (n = 267; 37%), with a dominant peak near 603 1047 1649 1734 White Rim Ss (11WRA; n = 90) 1441 Ma, dominate the sample set; nevertheless, this population is unequally 425 distributed between fluvial and eolian facies. The population composes 76% of 1648 White Rim Ss (11WRB; n = 84) 1036 1788 the two undifferentiated Cutler fluvial samples, in which the age range of grains,

1043 1372 1785 Upper Castle Valley Ss (10CVW; n = 93) ~1466–1406 Ma with one outlier at ca. 1349 Ma, is more restricted than the general population. The age range ~1466–1406 Ma is designated subpopulation 327 417 Lower Castle Valley Ss (10CVR; n = 90) 1025 1437 1738 D′. Population D makes up 27% of the Castle Valley Sandstone and 14% of the White Rim Sandstone samples. The main source for this grain age population 1442 Lower Castle Valley Ss (10CVG; n = 87) 451 in Laurentia is the 1.4 Ga granite-rhyolite suite that extends across the Yavapai 1052 1718 333 and Mazatzal basement provinces (Anderson, 1989; Dickinson and Gehrels, 2009). Potential local sources in the Uncompahgre uplift include the Vernal 422 Basal Castle Valley Ss (12CV50; n = 88) 1441 Mesa Monzogranite in Black Canyon (1434 ± 2 Ma, U-Pb zircon; Jessup et al.,

1041 1668 2006), texturally and mineralogically similar quartz monzonite in Unaweep Can- yon (1443 ± 22 Ma, U-Pb zircon; Bickford and Cudzilo, 1975), and cross-cutting 1438 Cutler fluvial (11CVC01; n = 100) pegmatite in Black Canyon (1413 ± 2 Ma, U-Pb zircon; Jessup et al., 2006). In the Needle Mountains of the San Juan dome, dated rocks in this age range include the Eolus Granite (1442 ± 3 Ma to 1435 ± 3 Ma, U-Pb zircon upper intercept; 1790–1689 Ma Gonzales and Van Schmus, 2007) and Trimble Granite (ca. 1350 Ma; Tewksbury, 1989). The latter age is represented by a single grain in the undifferentiated 1722 Cutler samples. Grains older than 1470 Ma in this population (n = 28), which are 1466–1406 Ma present in the White Rim and Castle Valley sandstones (Supplemental Table 1 [see footnote 1]), are not readily attributable to a local Uncompahgre source. 1445 Cutler fluvial (11CT01; n = 98)

Population E (~1288–900 Ma)

1726 This population of Late Mesoproterozoic to Early Neoproterozoic grains, referred to as Grenville grains, constitutes 17% of all grains analyzed in the 010002000 3000 4000 Cutler Group samples. It is common in all samples of the White Rim Sandstone Age (Ma) and Castle Valley Sandstone but is rare in the Cutler fluvial facies (n = 3). Grains of this age are typically attributed to ultimate derivation from the Grenville Figure 13. Normalized detrital-zircon plot for fluvial and eolian Cutler units in the Castle orogen of eastern Laurentia (e.g., Dickinson and Gehrels, 2009). Valley, Utah, and White Rim Sandstone in Canyonlands National Park and at Hite, Utah. Ex- planation: Cutler fluvial-facies samples 11CT01 from NE flank of Castle Valley and 11CVC01 from along Castle Creek at northwest end of Castle Valley. Castle Valley Sandstone samples are arranged in stratigraphic order. Lower two samples have slightly greater influence of Population F (~734–499 Ma) local sources than higher samples, indicated by narrow color bars indicating subpopulations D′ and C′. White Rim Sandstone samples are from Hite, Utah (11WRB), and Shafer Trail in Canyonlands National Park (11WRA). Sample of correlative Diamond Creek Sandstone is Late Neoproterozoic and Cambrian grains constitute 8% (n = 57) of grains from southeastern flank of Oquirrh basin in north-central Utah (Lawton et al., 2010). analyzed. This age range is common in all eolian samples but absent in the Cutler fluvial facies. This age group corresponds in part to the age range of volcanic rocks associated with Iapetan rifting along the eastern and southern 379; Jessup et al., 2006; Jones et al., 2009), with nearly unimodal age peaks margins of Laurentia (~765–530 Ma; Thomas, 2011, 2014), as well as Pan-Afri- in four samples at 1762 Ma, 1750 Ma, 1746 Ma, and 1740 Ma. Thus, known can basement domains in the Appalachian orogen and south of the Ouachita Proterozoic rock ages in the Uncompahgre uplift east of Castle Valley (Fig. 4) orogen (Mueller et al., 2014). Grains of this age are commonly associated and the San Juan dome to the southeast lie in the range of most zircon ages of with Grenville grains inferred to have an Appalachian source (Dickinson and subpopulation C′ in the fluvial Cutler Formation. Gehrels, 2003, 2009).

Population G (~491–283 Ma) petrography and detrital-zircon content indicate that the fluvial Cutler arkoses, at least in the upper part of the undifferentiated Cutler section, constitute an Paleozoic grains of this population, with a dominant peak at ca. 424 Ma, excellent example of locally sourced sediment. The detrital-zircon ages of the constitute 10% (n = 74) of all grains analyzed. They are present in subequal Cutler Formation have restricted ranges, ~1790–1689 Ma and ~1466–1406 Ma, quantities in all eolian samples, but only one grain (ca. 406 Ma) is present in subpopulations C′ and D′, respectively, which aggregate 98% of the two com- the Cutler fluvial samples. Grains of this age group are commonly attributed bined fluvial samples (Table 3). The other five grains (1349 Ma, 1195 Ma, to sources in peri-Gondwanan assemblages of the greater Appalachian orogen 1075 Ma, 960 Ma, and 406 Ma) are common components of the eolian strata (Dickinson and Gehrels, 2009) including the Taconic orogen (~490–440 Ma), and were likely blown into the fluvial system. The dominant age ranges cor- Acadian orogen (~420–350 Ma), and Alleghenian orogen (~330–270 Ma; e.g., respond to previously reported ages of metavolcanic, plutonic, and metasedi Thomas, 2011). A minor source for grains of this population might be present mentary rocks in the Unaweep and Black canyons, as discussed above, and in pre-Permian Paleozoic strata of the San Juan dome, although detrital-zircon thus provide additional insight into the ages and potential abundance of unex- data for these strata do not yet exist, and these ages are rare to absent in the posed Uncompahgre basement rocks. Although paleocurrent data in the Cut- Cutler fluvial-facies samples. There are no young grains near the depositional ler Formation indicate that sediment dispersal paralleled the salt walls, there age of the Cutler Group in the sample set. are low-elevation gaps in structural culminations of the diapirs, particularly the one between the Fisher Valley and Sinbad Valley diapirs (Fig. 4), which could have permitted rivers to cross major diapiric trends and deliver sediment to SANDSTONE PROVENANCE the Castle Valley area. Present data cannot preclude derivation from uplifted basement rocks farther to the southeast, for example in the vicinity of the San Detrital-zircon ages, sandstone petrology, and paleocurrent data indicate Juan dome, and detrital-zircon populations of local Cutler Formation strata in different sources for Cutler fluvial strata and the eolian samples of the study; Colorado should provide a basis for retaining or rejecting an exclusive nearby whereas the eolian White Rim and Castle Valley sandstones have composi- Uncompahgre source. tional similarities (Figs. 11–13). Moreover, stratigraphic trends in zircon age The lower eolianite member of the Castle Valley Sandstone contains a sig- populations indicate a lower percentage of locally derived grains in the upper nificant component of the local detritus as indicated by its subarkosic com- eolianite member of the Castle Valley Sandstone than in either the lower eoli- position and zircon population modes similar to those of the undifferentiated anite member or the undifferentiated Cutler Formation. The White Rim Sand- Cutler Formation; nevertheless, the locally derived zircons decrease in abun- stone contains a broad range of grain ages that resembles the distribution of dance upsection in the formation in concert with changing sandstone compo- grain ages in the upper eolianite unit and furthermore is similar to that of the sition (Table 3). The sample from the base of the eolianite (12CV50) contains correlative Diamond Creek Sandstone to the northwest (Figs. 1, 2, and 13). 7% and 19% grains in the age range ~1790–1689 Ma and ~1466–1406 Ma, The undifferentiated Cutler Formation consists of first-cycle arkose with subpopulations C′ and D′, respectively, a 71% decrease relative to the sum a bimodal zircon age population consisting of subpopulations C′ and D′ that of those subpopulations in the fluvial strata (Table 3). In contrast, grain pop- can be directly attributed to basement rocks of the Uncompahgre uplift. Thus, ulations scarce or absent in the fluvial samples dominate the basal eolian

TABLE 3. SUMMARY PERCENTAGES OF PETROGRAPHIC COMPONENTS AND DETRITAL-ZIRCON POPULATIONS C and D QtFL QtFL QmPK QmPK A and B (C′ and D′) E, F, and G Sample Stratigraphic unit (%Qt) (%F) (%P) (%K) (%) (%) (%) 06UT01 Diamond Creek Sandstone ND ND ND ND 739 (10) 52 11WRA White Rim Sandstone, Shafer Trail 91 82721 43 (13) 56 11WRB White Rim Sandstone, Hite 83 16 413938 (12) 51 10CVW Upper eolianite 88 12 4912 45 (13) 44 10CVG White lower eolianite 72 25 917851 (37) 41 10CVR Red lower eolianite 69 29 14 16 642 (23) 52 12CV50 Basal lower eolianite 69 27 920547 (26) 47 11CVC01 Cutler undiff, Castle Creek 54 45 14 32 098 (97) 2 11CT01 Cutler undiff, Castle Rock 61 37 16 21 098 (98) 2 Note: Population age ranges: A: 3539–2548 Ma; B: 2546–2008 Ma; C: 1991–1599 Ma; C′: 1790–1689 Ma; D: 1581–1302 Ma; D′: 1466–1406; E: 1288–900 Ma; F: 734–499 Ma; G: 491–283 Ma. Subpopulations C’ and D’ represent locally derived Uncompahgre grains. ND—not determined; undiff.—undifferentiated.

sample: younger populations E, F, and G constitute 47% of the sample, a 45% wall (Parriott basin of Banham and Mountney, 2013) and likely resulted in the increase relative to the fluvial samples; Archean and Paleoproterozoic popu- significant component of Uncompahgre detritus in the lower eolianite mem- lations A and B constitute 5% of the zircons analyzed. In higher samples of ber. With time, the northwest winds, more significant contributors to depo- the lower eolianite, populations E, F, and G similarly constitute 52% (sample sition of the upper member of the Castle Valley Sandstone, delivered large 10CVR) and 41% (sample 10CVG) of zircons analyzed, and populations A and volumes of far-traveled sediment to the proximal Paradox Basin. Although no B constitute 6% and 8% of the same samples, respectively. These numbers facies or transport data yet exist for the Diamond Creek Sandstone, it likely indicate that at least 50% of the zircons in the lower eolianite member were represents the updip edge of the erg near the marine margin of the Oquirrh delivered to the site by eolian transport. Compositional and zircon data indi- basin (e.g., Blakey, 2009). A shoreline source for White Rim sediment is sug- cate the White Rim Sandstone and the upper eolianite member contain com- gested by coarsening grain size westward toward the marine margin and inter parable populations of quartz, feldspar, and non-local zircon populations A, fingering of eolian and marine strata where they are exposed on the flank of B, E, F, and G, indicating that downwind drift of sediment in the greater White the Circle Cliffs uplift (Fig. 3; Kamola and Chan, 1988), and corroborated by Rim erg could have supplied essentially all detrital components of the upper the presence of glauconite grains and a crinoid fragment in the White Rim eolianite member. Sandstone in Canyonlands National Park (Steele-Mallory, 1982). Thus, the primary source for erg sediment was the Kungurian shoreline of western Pangea, as suggested by numerous previous workers (Johansen, 1988; Kamola and DISCUSSION Chan, 1988; Marzolf, 1988; Dubiel et al., 1996, 2009; Condon, 1997); nevertheless, the bimodal wind direction recorded in the upper eolianite member of the The Castle Valley Sandstone represents the innermost part of a shore- Castle Valley Sandstone evidently created large linear dunes whose remnant line-attached erg that extended in a downwind direction at least 250 km from topography is expressed on the upper surface of the White Rim Sandstone the southeastern flank of the Oquirrh basin to an exposed conspicuous, almost (Baars and Seager, 1970; Huntoon and Chan, 1987). linear, edge along the Colorado River and a buried, intricate edge in the salt The Namib erg of the West African coast (Fig. 14B) appears to be a reason- anticline province of the Paradox Basin (Fig. 14A), where small salt-withdrawal able analog for the White Rim erg. The modern African sand sea is affected basins enhanced local accommodation (Fig. 4). Extensively documented by a bimodal wind regime consisting of zonal SSE trade winds that blow off paleocurrents from the exposed southeastern edge of the erg (Baars and the Atlantic Ocean and seasonal easterly orographic winds, referred to as the Seager, 1970; Steele-Mallory, 1982; Huntoon and Chan, 1987) demonstrate berg (Bristow et al., 2007), that descend from the Great Escarpment (Fig. 14B; that northwesterly winds blew sand toward its current pinch out; data pre- Glennie, 1987). The central part of the Namib erg consists of prominent linear sented here indicate that those winds transported sediment along the axes dunes with north-south crests that extend for over 100 km in some examples of the salt-withdrawal basins. Although the present erg margin that parallels (Fig. 14B). These complex linear dunes (Bristow et al., 2007) are analogues the Colorado River has been interpreted as an erosional pinch out beneath for the linear features preserved on the surface of the White Rim Sandstone. the Moenkopi Formation (Dubiel et al., 1996, 2009; Huntoon et al., 2002), the Fluvial deposits of the interdune member separate the upper and lower current margin probably does not lie far from its original depositional pinch eolianite members of the Castle Valley Sandstone and approximately coincide out for the following reasons: (1) The pinch-out margin trends perpendicular with a shift to more mature sandstone compositions. Fluvial deposition is indi- to dominant direction of Permian sand transport, supporting the inference of cated by the presence of an irregular scoured base, pebble lags, and horizontal sediment depletion with transport distance (e.g., Chan, 1989); (2) the White laminae interpreted as sheet-flood deposits. The source of the sediment was Rim Sandstone thins on the order of 700 m across eastern Utah subparallel to the topographically elevated salt wall and its flanking strata. Dolomite clasts the trend of the pinch out (Fig. 4), which is not likely due solely to pre-Triassic were derived from the diapir itself, which was exposed during deposition of beveling; (3) dominant large-scale trough cross-beds and curved dune crests the eolian strata and superjacent Moenkopi beds (Fig. 9F; Lawton and Buck, at our Shafer Trail sample locality (also noted by Dubiel et al., 1996) indicate 2006), whereas granite and quartz pebbles were derived from exposed con- deposition by barchan dunes and hence diminished sand supply directly up- glomeratic Cutler beds upturned adjacent to the diapir (Fig. 9F). Fluvial depo- wind of the White Rim pinch out. The downwind erg margin appears to have sition may have been triggered by a transient shift to a seasonally wet climate, advanced farther southeast in the foredeep of the Paradox Basin as a result of as has been suggested for progradation of the Organ Rock Formation above continued subsidence and the effect of salt withdrawal (Fig. 14A). Sand that the Cedar Mesa Sandstone (Stanesco et al., 2000; Mountney, 2006; Dubiel occupied the salt-withdrawal basins was reworked extensively during its ini- et al., 2009). Because of the great distances to the time-equivalent marine tial arrival by northeast winds that represent either the general Pangean zonal shoreline, ~250 km upwind and ~100 km directly normal to the shoreline, it trade winds (Parrish and Peterson, 1988; Peterson, 1988) or local foehn winds is unlikely that bounding surfaces within the eolian succession were gener- that blew off the high-standing Uncompahgre uplift. The northeasterlies de- ated by water-table changes driven by glacial eustasy, as suggested for Cedar flated sand from the salt-withdrawal basin northeast of the Castle Valley salt Mesa bounding surfaces (Mountney, 2006). Rather, water table fluctuations

AB0 100 km

DC West Pangean Seaway Uncompahgre uplift

W h i te

Escarpment

Atlantic Ocean R im

Namib Sand Sea

Deflated

chenier e r plain CR g

Permian Great North North Organ Rock alluvial plain Kuiseb

Edge Pennsylvanian North ND salt Alluvial Rive 0 100 km plain r Walvis Bay

Figure 14. (A) Reconstruction of White Rim erg during Kungurian (late Leonardian, ca. 273 Ma) time. Black arrows are average estimated wind directions from White Rim Sandstone foresets discussed in text. Red arrow is average foreset dip direction of Huntoon and Chan (1987). Violet arrows are wind directions estimated from dominant foreset dip in lower member of Castle Valley Sandstone. Dashed black arrow near shoreline is estimated direction of longshore drift driven by NNW winds. Thin arrows are sediment transport directions estimated from fluvial cross-bed data of the undifferentiated Cutler Formation (Buller, 2009; Venus et al., 2015) and Organ Rock Formation (arrow east of confluence of Green and Colorado rivers; Mountney and Jagger, 2004) and provenance data described in this paper. Thin black lines near confluence of Green and Colorado rivers are linear topographic features on upper surface of White Rim Sandstone (Baars and Seager, 1970), here interpreted as remnant topography created by large linear dunes. They appear short on the map because they are only exposed on the surface of the White Rim Sandstone and are buried to the northwest beneath the Moenkopi Formation. Shoreline position from 275 Ma map in Blakey (2009). Position of Diamond Creek Sandstone sample (DC) adjusted 30 km westward to accommodate eastward translation during Late Cretaceous shortening (Kwon and Mitra, 2004). Other locations: CR—Capitol Reef shoreline location (Kamola and Chan, 1988); ND—Nokai Dome, where 7 m of White Rim Sandstone is interpreted to overlie a separate erg deposit, the De Chelly Sandstone (Irwin, 1971). (B) Modern Namib sand sea (note north orientation), illustrating dominant south-southwesterly zonal trade wind direction (black arrows) and orographic berg wind direction (violet arrow). Wind directions from Glennie (1987); base map from GoogleEarth. Thin black lines are prominent linear dunes in central part of erg; thin black arrows indicate fluvial dispersal directions.

and shifts in the associated capillary fringe were likely caused by short-term seems to corroborate similarity of process, suggesting that the persistent color climatic cyclicity in combination with high sediment-accumulation rates in the change in the Castle Valley sandstone is also a result of hydrocarbon migration adjacent salt-withdrawal minibasin. through the sandstone. Moreover, the sandstone composition and detrital- White intervals of Castle Valley Sandstone are similar petrographically zircon content of the white parts of the sandstone contrast with that of the pink to bleached facies of the White Rim Sandstone in parts of the greater White part, suggesting that hematite cementation may have been in part controlled Rim erg that have been attributed to leaching of previously deposited hema- by the presence or absence of detrital iron oxide grains in the arkosic sand- tite cement by hydrocarbons (Gorenc and Chan, 2015). The presence of de- stones. Why the color change conforms closely to lithostratigraphy in the tilted graded hydrocarbon in the white parts of the Castle Valley Sandstone (Fig. 7F) sandstone and why it is truncated beneath the Moenkopi Formation remain

open questions, which nevertheless suggest that the hydrocarbons were pres- quent long-distance tectonic transport along one or the other margins of Lau- ent in the rocks in the Permian. rentia (Wright and Wyld, 2006; Grove et al., 2008) and now occupying oceanic The diverse grain ages of the Castle Valley and White Rim Sandstone re- crustal domains west of the study area in northern California. Rocks in the semble population assemblages that have been attributed to sources in the age range 1.6–1.5 Ga are also present in the Amazonian craton (e.g., Cordani Appalachian orogen of eastern Laurentia. In particular these assemblages et al., 2009; Cardona et al., 2010), and have been posited as a possible source include Grenville, Neoproterozoic, and early Paleozoic grain ages attributed for grains in Permian sandstones of southwestern Laurentia (Soreghan and to 1.1 Ga Grenville granites, pan-African crust (Suwannee terrane), and peri- Soreghan, 2013). Gondwanan terranes, respectively, in the Appalachian region and in the sub- General paleogeographic arguments against Permian sediment delivery surface south of the Ouachita orogen (e.g., Viele and Thomas, 1989; Mueller from Cordilleran accreted terranes and from the suture between Gondwana et al., 2014), and present in other Permian eolian sandstones, including the and Laurentia were presented by Dickinson and Gehrels (2003), who favored Coconino Sandstone, of southwestern Laurentia (Dickinson and Gehrels, 2003; transcontinental fluvial sediment delivery to the Laurentian marine margin Gehrels et al., 2011). These grains were likely delivered by transcontinental coupled with longshore transport driven by zonal trade winds and deflation fluvial systems to the Permian shoreline NW of the Ancestral Rocky Mountain of coastal plain sediment into the Early Permian erg (Fig. 1). Those authors province and transported by eolian processes into the Permian ergs of western objected to sediment sources to the west on the basis of the intervening Penn- Pangea (Johansen, 1988; Marzolf, 1988; Dickinson and Gehrels, 2003; Gehrels sylvanian–Permian marine sedimentary basins on the western margin of Lau- et al., 2011). This hypothesis is consistent with the prevailing data that indicate rentia that would have blocked sediment transport from western sources, and that the greater White Rim erg was deposited by winds that blew from the sediment sources to the south were rejected on the basis of an assemblage northwest, away from the shoreline. of marine foreland basins that lay north of the Ouachita-Marathon suture belt Northwesterly winds, rather than zonal northeasterly trade winds (Parrish in Texas and New Mexico. Whereas the eastern components of this foreland and Peterson, 1988; Peterson, 1988), thus dominated eolian sand transport in basin system ceased to subside in the Early Permian (Ingersoll et al., 1995; the White Rim erg. Given the long distance of transport from the Kungurian Dickinson and Lawton, 2003; Thomas, 2014), remnant topography of the su- marine margin in north-central Utah, it seems likely that a seasonal, or mon- ture zone was likely effective at blocking sediment delivery from the low-lying soonal, low-pressure system over Gondwana was the driver of the northwest- Amazonian shield. erly circulation pattern, as predicted by Parrish and Peterson (1988), rather Zircon grains in Permian eolian strata of the Paradox Basin with likely than onshore breezes. Whereas a high-standing Uncompahgre uplift might Pan-African affinity (~765–535 Ma) and sources in eastern and southeastern have created fierce topographic winds in the proximal part of the Paradox Laurentia provide additional leverage on ultimate sources of grains in the Basin, it might have sheltered the more distal part of the basin from zonal trade White Rim erg. Grains in this age range constitute 4%–11% of the six sam- winds that dominated sand transport in the approximately time-equivalent ples of eolian strata sampled in this study and 4% of grains in the Diamond De Chelly and Coconino ergs (Peterson, 1988). In addition, the northwesterly Creek Sandstone (Lawton et al., 2010). In contrast, this age range is absent to winds appear to have resulted in large erg deposits on the windward side of rare (generally <1%) in accreted eugeoclinal strata of northern California and the large peninsula that straddled the transcontinental arch (Fig. 1) and lesser related oceanic terranes, which include both lower Paleozoic strata and plu- sand accumulations on the leeward, southeastern side of the peninsula (e.g., tonic rocks, to the north in British Columbia and southeastern Alaska (Gehrels Blakey, 2009). et al., 1996; Grove et al., 2008). Pan-African grains could therefore not have Grains in the age range 1607–1492 Ma (n = 26 or 4% of all analyses), which been derived from the Cordilleran terranes on the basis of existing data; form a subset of population D and fall within the postulated North American nevertheless, because Pan-African grains are likewise uncommon in Baltica- magmatic gap (~1.61–1.49 Ga; Van Schmus et al., 1993; Grove et al., 2008), derived sandstones (e.g., Bingen and Solli, 2009), Permian eolian sandstones are difficult to explain by appealing to Laurentian basement sources. Zircon containing both Pan-African and Baltica-derived grains in any event require a grains in the age range ~1.61–1.49 Ga are present in all Kungurian eolian strata combination of sediment-dispersal systems that transported sediment from of this study in abundances ranging from 2% to 13% of each sample analyzed different parts of Laurentia. These separate systems could have been: (1) trans- (Supplemental Table 1 [see footnote 1]) and 7% of the correlative Diamond continental drainages with headwaters in the former Caledonian orogen and Creek Sandstone of north-central Utah (Lawton et al., 2010). Grains in this age farther south along the Appalachian orogen and even the Ouachita orogen, range could have been derived directly from continental sources on the west- to tap northern sources of Baltica and Pinwarian crust and southern sources ern edge of Baltica, present in the early Paleozoic Caledonian suture between containing crust of Pan-African affinity, respectively; or (2) transcontinental Baltica and Laurentia (e.g., Bingen and Solli, 2009) and the Pinware terrane sources with headwaters in the Pan-African crustal sources of the Appalachian of SE Labrador (Tucker and Gower, 1994; Wasteneys et al., 1997), or from region and shorter sediment-transport systems with headwaters in the west, western accreted terranes that contain zircon grains and basement fragments which somehow bypassed the western marine basins of western Laurentia. possibly derived from the Caledonian orogen by tectonic escape and subse- The former paleogeographic model is preferred here, consisting of westward-

and southwestward-directed transcontinental fluvial systems that transported picted the De Chelly as somewhat older than the White Rim (Blakey 1990, 1996; sediment from varied northeastern and eastern sources in the Caledonian and Dubiel et al., 2009). Like the lower eolianite member of the Castle Valley Sand- Appalachian orogens to a marine mixing zone along the Permian shoreline of stone, the De Chelly Sandstone has prominent paleocurrent indicators to the Utah, Idaho, and Montana, from which the sands were delivered to the Para- SW and SE (Stanesco, 1991; Peterson, 1988), and examination of a single thin dox Basin. section from the Laramide Defiance uplift on the Arizona–New Mexico state Salt tectonics within the salt anticline province provided critical influence line (Pennsylvanian Zuni uplift of Fig.1) indicates that it contains as much as on local eolian sediment transport and accumulation of eolian sand, as well 20% potassium feldspar, including microcline, a compositional characteristic as the facies distribution and composition of the sand, in the Paradox Basin. of the lower eolianite member. Future detrital-zircon analysis of the De Chelly Rapid subsidence within salt-withdrawal minibasins in the northwestern part Sandstone might provide improved insight into possible correlation with the of the salt anticline province provided accommodation for eolian sand at the lower eolianite member of the Castle Valley Sandstone. same time as topographically expressed salt walls created protected leeward sites for sand accumulation. Indeed, some of the thickest eolian sand accumulations lie in the Big Bend minibasin southwest of the Castle Valley salt CONCLUSIONS wall (Fig. 4). The initial eolian sediment contained a significant component of first-cycle arkose derived directly from the Uncompahgre uplift and depos- Prominent exposures of Lower Permian (Kungurian and upper Leonardian) ited on the leeward side of the salt wall as recorded by the lower eolianite eolian sandstone on the flank of the Castle Valley salt wall were deposited at member. With time, and deposition of the upper eolianite member, northwest the top of the Cutler Group in the northeastern part of the Paradox Basin in a winds evidently became more influential and provided a greater percentage, salt withdrawal sub-basin. Termed here the Castle Valley Sandstone, the eo- roughly 100%, of sediment derived from the Laurentian marine margin. At lian deposits are continuous in the subsurface with, and constitute the depo this time, eolian sediment accumulation greatly outpaced supply from local sitional edge of, an extensive erg recorded by the time-equivalent White Rim fluvial systems, which could have resulted from decreased uplift rate of the Sandstone. The greater White Rim erg extended 125–150 km east from the Uncompahgre source (e.g., Soreghan et al., 2009) or high rate of sediment time-equivalent edge of the west Pangean seaway, the shoreline of which supply to the White Rim erg, an alternative possibility suggested by the gen- trended approximately north-south, and at least 250 km downwind of littoral eral absence of interfingering of fluvial and eolian facies noted by White Rim sediment sources on the southeastern flank of the Oquirrh basin. The Castle stratigraphers (e.g., Huntoon and Chan, 1987; Chan, 1989). Eolian sediment Valley Sandstone, as much as 183 m thick in outcrop, consists of two informal transport was impeded to farther southeastern minibasins in the salt anticline eolianite members separated by a fluvial deposit termed the interdune mem- province by a topographic obstruction near the intersection of the plunging ber. The upper part of the lower member and the upper member are bleached nose of the Castle Valley salt wall and the west-trending Cache Valley salt wall. by hydrocarbons that once occupied the eolian sandstone. The Castle Valley Although reasons for the increased importance of northwest winds remain Sandstone overlies fluvial red beds of the undifferentiated Cutler Formation, unclear, the corresponding compositional change in the White Rim Sandstone which may be equivalent to the Organ Rock Formation of the southwestern occurred just prior to deposition of the interdune member in the middle of part of the Paradox Basin. the formation. It seems likely that the change in local depositional style, from Provenance of fluvial and eolian Cutler Group strata reflects a combination eolian to fluvial deposition, followed by a return to eolian deposition with of local and distant erosional sources. Cutler fluvial strata are compositional

a stronger component of transport from the northwest, might signal an im- arkoses with average composition Qt56F42L2 and a narrowly defined bimodal portant change in the climate of western Pangea, perhaps due to increasing detrital-zircon content with modes at ca. 1724 Ma and ca. 1441 Ma. The arkose strength of the southern low-pressure system over Gondwana (e.g., Parrish was derived entirely from Proterozoic basement of the nearby Uncompahgre and Peterson, 1988). uplift, located no more than 40 km from the depositional site. Castle Valley The great thickness of the Castle Valley Sandstone in the Big Bend mini- Sandstone compositions change stratigraphically toward increased maturity basin (Fig. 4), the difference in dominant wind directions between lower and with height in the section. The unbleached part of the lower member is quartz-

upper eolianite members, and the compositional difference between the mem- rich arkose (Qt71F27L2) with a zircon population that includes Archean, Gren- bers combine to suggest the possibility that the Castle Valley Sandstone may ville, Neoproterozoic, and Early Proterozoic grains, ages not present in known correlate with both the White Rim Sandstone and the De Chelly Sandstone of basement of the Uncompahgre uplift, in addition to grains equivalent in age the Four Corners region (R.F. Dubiel, 2015, written commun.), as suggested in to the locally derived Uncompahgre zircons. The lower member was trans- Figure 2. Formerly considered equivalent to the White Rim Sandstone (Baars, ported in part by northeasterly winds that picked up sediment from the Cutler 1962), the De Chelly Sandstone was later interpreted to underlie the White Rim fluvial plain and deposited it on the lee (southwest) side of the salt wall. The Sandstone in an exploration well at Nokai Dome on the San Juan River (Figs. upper member of the Castle Valley Sandstone, deposited following an episode 3 and 14; Irwin, 1971); accordingly subsequent correlations have generally de- of sheet-flood deposition recorded by the interdune member, has an average

REFERENCES CITED composition Qt90F10L0, a detrital-zircon content that completely lacks locally derived grains but contains abundant Grenville, Neoproterozoic (Pan-African), Anderson, J.L., 1989, Proterozoic anorogenic granites of the southwestern United States, in and early Paleozoic grains, as well as some grains in the range ~1.61–1.49 Ga Jenney, J.P., and Reynolds, S.J., eds., Geologic Evolution of Arizona: Tucson, Arizona Geologi cal Society Digest 17, p. 211–238. that are here attributed to an ultimate source in Baltica. The upper member Baars, D.L., 1962, Permian System of the Colorado Plateau: The American Association of Petro- was deposited by a combination of northeasterly and northwesterly winds, the leum Geologists Bulletin, v. 46, p. 149–218. latter similar to the predominant wind direction recorded in the greater White Baars, D.L., 1966, Pre-Pennsylvanian paleotectonics—Key to basin evolution and petroleum oc- currences in Paradox Basin, Utah and Colorado: The American Association of Petroleum Rim erg. The detrital-zircon content of the White Rim Sandstone, sampled at Geologists Bulletin, v. 50, p. 2082–2111. two localities to the southwest, resembles that of the upper member of the Baars, D.L., and Seager, W.R., 1970, Stratigraphic control of petroleum in White Rim Sandstone Castle Valley Sandstone. (Permian) in and near Canyonlands National Park, Utah: The American Association of Petro- leum Geologists Bulletin, v. 54, p. 709–718. As suggested by previous authors, sediment was transported via trans Baars, D.L., and Stevenson, G.M., 1981, Tectonic evolution of the Paradox Basin, Utah and Colo continental rivers to the western marine margin of Laurentian Pangea from the rado, in Wiegand, D.L., ed., Geology of the Paradox Basin: Rocky Mountain Association of Appalachian region, which provided Grenville, Pan-African, and lower Paleo Geologists, Field Conference, Guidebook, p. 23–31. Baker, A.A., Dane, C.H., and Reeside, J.B., Jr., 1933, Paradox Formation of eastern Utah and west- zoic grains to the littoral zone. In addition, northern tributaries to the transcon- ern Colorado: The American Association of Petroleum Geologists Bulletin, v. 17, p. 963–980. tinental drainage, or a separate fluvial trunk river lying to the north, drained Banham, S.G., and Mountney, N.P., 2013, Controls on fluvial sedimentary architecture and sedi- remnant topography of the early Paleozoic Caledonian orogeny, or nearer ment-fill state in salt-walled mini-basins: Triassic Moenkopi Formation, salt anticline region, sources in Labrador, to supply grains of Baltica affinity. Baltica-age grains did SE Utah, USA: Basin Research, v. 25, p. 709–737, doi:10.1111 /bre.12022. Banham, S.G., and Mountney, N.P., 2014, Climatic versus halokinetic control on sedimentation in not derive from accreted terranes in the Cordillera due to the intervening ma- a dryland fluvial succession: Sedimentology, v. 61, p. 570–608, doi:10.1111 /sed.12064. rine sedimentary basins that lay between the western shoreline of Laurentia Barbeau, D.L., 2003, A flexural model for the Paradox Basin: Implications for the tectonics of the and the potential Cordilleran terranes, which moreover lack Neoproterozoic Ancestral Rocky Mountains: Basin Research, v. 15, p. 97–115, doi:10.1046/j.1365-2117.2003 .00194.x. Pan-African grains. Abundant sediment was blown southeastward from littoral Bickford, M.E., and Cudzilo, T.F., 1975, U-Pb age of zircon from Vernal Mesa–type quartz mon sources incrementally exposed during Kungurian sea-level drawdown. Rapid zonite, Unaweep Canyon, west-central Colorado: Geological Society of America Bulletin, transport of voluminous eolian sediment overwhelmed sediment derived from v. 86, p. 1432–1434, doi:10.1130/0016-7606(1975)86<1432:UAOZFV>2.0.CO;2. Bickford, M.E., Shuster, R.D., and Boardman, S.J., 1989, U-Pb geochronology of the Proterozoic local Uncompahgre sources and resulted in observed compositional changes volcano-plutonic terrane in the Gunnison and Salida areas, Colorado, in Grambling, J.A., and in eolian relative to fluvial sediment. Tewksbury, B.J., eds., Proterozoic Geology of the Southern Rocky Mountains: Geological So- A combination of high subsidence rates and topographic expression of salt ciety of America Special Paper 235, p. 33–48. Bingen, B., and Solli, A., 2009, Geochronology of magmatism in the Caledonian and Sveconor- walls, both induced by salt diapirism in the northeastern part of the Paradox wegian belts of Baltica: Synopsis for detrital zircon provenance studies: Norwegian Journal Basin, permitted preservation of the rapidly introduced eolian sediment, which of Geology, v. 89, p. 267–290. might otherwise have simply been deflated to more distant sites, on the in- Bissell, H.J., 1962, Permian rocks of parts of Nevada, Utah, and Idaho: Geological Society of America Bulletin, v. 73, p. 1083–1110, doi:10.1130/0016-7606(1962)73[1083:PROPON]2.0.CO;2. board flank of the White Rim erg. Consideration of basin-scale paleocurrent Blair, T.C., and McPherson, J.G., 1994, Alluvial fans and their natural distinction from rivers based patterns, sandstone composition from traditional petrographic methods, and on morphology, hydraulic processes, sedimentary processes, and facies assemblages: Jour- detrital-zircon content of the Early Permian depositional system thus demon- nal of Sedimentary Research, v. A64, p. 450–489. strates the importance of regional transport systems in creating large volumes Blakey, R.C., 1990, Permian eolian deposits, sequences, and sequence boundaries, Colorado Pla- teau, in Longman, M.W., and Sonnenfeld, M.D., eds., Paleozoic Systems of the Rocky Moun- of far-traveled sediment in a local basin setting. tain Region: Rocky Mountain Section SEPM (Society for Sedimentary Geology), p. 405–426. Blakey, R.C., 1996, Permian eolian deposits, sequences, and sequence boundaries, Colorado Pla- teau, in Longman, M.W., and Sonnenfeld, M.D., eds., Paleozoic Systems of the Rocky Moun- tain Region: Rocky Mountain Section SEPM (Society for Sedimentary Geology), p. 405–426. ACKNOWLEDGMENTS Blakey, R.C., 2009, Paleogeography and geologic history of the western Ancestral Rocky Moun- We thank local landowners Jay Zuckerman and Randall Jorgen for access to outcrops at the north tains, Pennsylvanian–Permian, southern Rocky Mountains and Colorado Plateau, in Houston, end of Castle Valley. Field and analytical work was funded in part by the Institute of Tectonic Stud- W.S., Wray, L.L., and Moreland, P.G., eds., The Paradox Basin Revisited—New Developments ies, a joint industry consortium for the study of salt sediment-interaction, formerly located at New in Petroleum Systems and Basin Analysis: Rocky Mountain Association of Geologists, Special Mexico State University. Thorough reviews by Russ Dubiel and Bill Thomas greatly improved Paper (CD-ROM), p. 222–264. manuscript clarity and interpretations. We acknowledge discussions of local geology, regional re- Blakey, R.C., Peterson, F., and Kocurek, G., 1988, Synthesis of late Paleozoic and Mesozoic eolian lations, and salt tectonics with Bill Dickinson, Kate Giles, Thomas Hearon, Steve Holdaway, Chuck deposits of the Western Interior of the United States: Sedimentary Geology, v. 56, p. 3–125, Kluth, Don Rasmussen, Mark Rowan, Austin Shock, and Bill Thomas. Mark Pecha and Victor Valen- doi:10.1016/0037-0738(88)90050-4. cia provided 24-hour support and assistance at the University of Arizona LaserChron Laboratory, Bristow, C.S., Duller, G.A.T., and Lancaster, N., 2007, Age and dynamics of linear dunes in the which was supported by National Science Foundation grant EAR-0732436. Todd Parr, Ed Bauer, Namib Desert: Geology, v. 35, p. 555–558, doi:10.1130 /G23369A .1. Chris Clinkscales, and William Schellenbach assisted with detrital-zircon analyses. Lawton further Buller, C.D., 2009, The influence of salt on stratigraphy and depositional environments of the gratefully acknowledges the hospitality of Kaaron and Randy Jorgen of Castle Valley and an edi- Pennsylvanian–Permian Honaker Trail and Cutler formations, Paradox Basin, Utah [M.S. fying Castle Valley overflight by long-time friend Scott Fasken. We thank officials of Canyonlands thesis]: Las Cruces, New Mexico State University, 91 p. National Park and Glen Canyon National Recreation Area for permission to sample the White Rim Campbell, J.A., 1979, Lower Permian deposition system, northern Uncompahgre basin, in Baars, D.L., Sandstone. ed., Permianland: Four Corners Geological Society, 9th Field Conference, Guidebook, p. 13–21.

Campbell, J.A., 1980, Lower Permian depositional systems and Wolfcampian paleogeography, Gehrels, G.E., and Pecha, M., 2014, Detrital zircon U-Pb geochronology and Hf isotope geochem- Uncompahgre basin, eastern Utah and southwestern Colorado, in Fouch, T.D., and Magathan, istry of Paleozoic and Triassic passive margin strata of western North America: Geosphere, E.R., eds., Paleozoic Paleogeography of the West-Central United States: Rocky Mountain Sec- v. 10, p. 49–65, doi:10.1130/GES00889.1. tion SEPM (Society for Sedimentary Geology), p. 327–340. Gehrels, G.E., Butler, R.F., and Bazard, D.R., 1996, Detrital zircon geochronology of the Alexander Cardona, A., Chew, D., Valencia, V.A., Bayona, G., Miškovic´, A., and Ibañez-Mejía, M., 2010, Gren- terrane, southeastern Alaska: Geological Society of America Bulletin, v. 108, p. 722–734, doi: villian remnants in the northern Andes: Rodinian and Phanerozoic paleogeographic per- 10.1130/0016-7606(1996)108<0722:DZGOTA>2.3.CO;2. spectives: Journal of South American Earth Sciences, v. 29, p. 92–104, doi:10.1016 /j .jsames Gehrels, G.E., Valencia, V.A., and Ruiz, J., 2008, Enhanced precision, accuracy, efficiency, and .2009.07.011. spatial resolution of U-Pb ages by laser ablation–multicollector–inductively coupled Cater, F.W., and Elston, D.P., 1963, Structural development of salt anticlines of Colorado and Utah, plasma–mass spectrometry: Geochemistry Geophysics Geosystems, v. 9, Q03017, doi:10 in Childs, O.E., and Beebe, B.W., eds., Backbone of the Americas—Tectonic History from Pole .1029/2007GC001805. to Pole: American Association of Petroleum Geologists Memoir 2, p. 152–159. Gehrels, G.E., Blakey, R., Karlstrom, K.E., Timmons, J.M., Dickinson, B., and Pecha, M., 2011, Chan, M.A., 1989, Erg margin of the Permian White Rim Sandstone, SE Utah: Sedimentology, Detrital zircon U-Pb geochronology of Paleozoic strata in the Grand Canyon, Arizona: Litho- v. 36, p. 235–251, doi:10.1111/j.1365-3091.1989.tb00605.x. sphere, v. 3, p. 183–200, doi:10.1130/L121.1. Condon, S.M., 1997, Geology of the Pennsylvanian and Permian Cutler Group and Permian Kaibab Geslin, J.K., 1998, Distal Ancestral Rocky Mountains tectonism: Evolution of the Pennsylvanian– Limestone in the Paradox Basin, southeastern Utah and southwestern Colorado: U.S. Geologi Permian Oquirrh–Wood River basin, southern Idaho: Geological Society of America Bulletin, cal Survey Bulletin 2000-P, 55 p. v. 110, p. 644–663, doi:10.1130/0016-7606(1998)110<0644:DARMTE>2.3.CO;2. Cordani, U.G., Teixeira, W., D’Agrella-Filho, M.S., and Trindade, R.I., 2009, The position of the Giles, K.A., and Lawton, T.F., 2002, Halokinetic sequence stratigraphy adjacent to the El Papalote Amazonian Craton in supercontinents: Gondwana Research, v. 15, p. 396–407, doi:10.1016 /j diapir, northeastern Mexico: The American Association of Petroleum Geologists Bulletin, .gr.2008.12.005. v. 86, p. 823–840. DeVoto, R., 1980, Pennsylvanian stratigraphy and history of Colorado, in Kent, H.C., and Porter, Giles, K.A., and Rowan, M.G., 2012, Concepts in halokinetic-sequence deformation and stratig- K.W., eds., Proceedings, 1980 Symposium on Colorado Geology: Rocky Mountain Association raphy, in Alsop, G.I., Archer, S.G., Hartley, A.J., Grant, N.T., and Hodgkinson, R., eds., Salt of Geologists, p. 71–101. Tectonics, Sediments and Prospectivity: Geological Society of London Special Publication 363, Dickinson, W.R., and Gehrels, G.E., 2003, U-Pb Ages of detrital zircons from Permian and Jurassic p. 7–31. eolian sandstones of the Colorado Plateau, USA: Paleogeographic implications: Sedimen- Glennie, K.W., 1987, Desert sedimentary environments, present and past—A summary: Sedimen- tary Geology, v. 163, p. 29–66, doi:10.1016/S0037-0738(03)00158-1. tary Geology, v. 50, p. 135–165, doi:10.1016/0037-0738(87)90031-5. Dickinson, W.R., and Gehrels, G.E., 2009, U-Pb ages of detrital zircons in Jurassic eolian and Goldhammer, R.K., Oswald, E.J., and Dunn, P.A., 1994, High-frequency, glacio-eustatic cyclicity in associated sandstones of the Colorado Plateau: Evidence for transcontinental dispersal and the middle Pennsylvanian of the Paradox Basin: An evaluation of Milankovitch forcing: Inter- intraregional recycling of sediment: Geological Society of America Bulletin, v. 121, p. 408– national Association of Sedimentologists Special Publication, v. 19, 243–283 p. 433, doi:10.1130/B26406.1. Gonzales, D.A., and Van Schmus, W.R., 2007, Proterozoic history and crustal evolution in south- Dickinson, W.R., and Lawton, T.F., 2003, Sequential intercontinental suturing as the ultimate con- western Colorado: Insight from U/Pb and Sm/Nd data: Precambrian Research, v. 154, p. 31– trol for Pennsylvanian Ancestral Rocky Mountains deformation: Geology, v. 31, p. 609–612. 70, doi:10.1016/j.precamres.2006.12.001. Doelling, H.H., 1988, Geology of Salt Valley anticline and Arches National Park, Grand County, Gorenc, M.A., and Chan, M.A., 2015, Hydrocarbon-induced diagenetic alteration of the Permian Utah, in Doelling, H.H., Oviatt, C.G., and Huntoon, P.W., eds., Salt Deformation in the Paradox White Rim Sandstone, Elaterite Basin, southeast Utah: The American Association of Petro- Region: Utah Geological and Mineral Survey Bulletin 122, p. 1–58. leum Geologists Bulletin, v. 99, p. 807–829, doi:10.1306 /10081413128 . Doelling, H.H., 2002a, Geologic map of the Moab and the eastern part of the San Rafael Desert Gradstein, F.M., Ogg, J.G., Schmitz, M.D., and Ogg, G.M., 2012, The Geologic Time Scale 2012: 30′ × 60′ quadrangles, Grand and Emery Counties, Utah, and Mesa County, Colorado: Utah Boston, Elsevier, 1144 p. Geological and Mineral Survey Map 180, scale 1:100,000, 3 sheets. Grove, M., Gehrels, G.E., Cotkin, S.J., Wright, J.E., and Zou, H., 2008, Non-Laurentian cratonal Doelling, H.H., 2002b, Geologic map of the Fisher Towers 7.5′ quadrangle, Grand County, Utah, provenance of Late Ordovician eastern Klamath blueschists and a link to the Alexander terrane, Utah Geological Survey Map 183, scale 1:24,000, 2 sheets, 22 p. in Wright, J.E., and Shervais, J.W., eds., Ophiolites, Arcs, and Batholiths: A Tribute to Cliff Hop- Doelling, H.H., and Ross, M.L., 1998, Geologic map of the Big Bend quadrangle, Grand County, son: Geological Society of America Special Paper 438, p. 223–250, doi: 10.1130/2008.2438(08). Utah, Utah Geological Survey Map 171, scale 1:24,000, 2 sheets. Hatcher, R.D., Jr., 1989, Tectonic synthesis of the U.S. Appalachians, in Hatcher, R.D., Jr., Thomas, Dubiel, R.F., Huntoon, J.E., Condon, S.M., and Stanesco, J.D., 1996, Permian deposystems, paleo W.A., and Viele, G.W., eds., The Appalachian-Ouachita Orogen in the United States: Geological geography, and paleoclimate of the Paradox Basin and vicinity, in Longman, M.W., and Son- Society of America, The Geology of North America, v. F-2, p. 511–535. nenfeld, M.D., eds., Paleozoic Systems of the Rocky Mountain Region: Rocky Mountain Sec- Hill, B.M., and Bickford, M.E., 2001, Paleoproterozoic rocks of central Colorado: Accreted arcs or tion SEPM (Society for Sedimentary Geology), p. 427–443. extended older crust?: Geology, v. 29, p. 1015–1018, doi:10.1130/0091-7613(2001)029<1015: Dubiel, R.F., Huntoon, J.E., Stanesco, J.D., and Condon, S.M., 2009, Cutler Group alluvial, eo- PROCCA>2.0.CO;2. lian, and marine deposystems: Permian facies relations and climatic variability in the Paradox Hintze, L.F., 1988, Geologic history of Utah: Brigham Young University Geology Studies Special Basin, in Houston, W.S., Wray, L.L., and Moreland, P.G., eds., The Paradox Basin Revisited— Publication 7, 202 p. New Developments in Petroleum Systems and Basin Analysis: Rocky Mountain Association Hite, R.J., 1970, Shelf carbonate sedimentation controlled by salinity in the Paradox Basin, south- of Geologists, Special Publication, p. 265–308. east Utah, in Ron, J.L., and Dellwig, L.F., eds., Third Symposium on Salt, Volume 1, Northern Elston, D.P., Shoemaker, E.M., and Landis, E.R., 1962, Uncompahgre front and salt anticline re- Ohio Geologic Society, p. 48–66. gion of Paradox Basin, Colorado and Utah: The American Association of Petroleum Geolo- Hite, R.J., and Buckner, D.H., 1981, Stratigraphic correlations, facies concepts, and cyclicity in gists Bulletin, v. 46, p. 1857–1878. Pennsylvanian rocks of the Paradox Basin, in Wiegand, D.L., ed., Geology of the Paradox Ba- Frahme, C.W., and Vaughn, E.B., 1983, Paleozoic geology and seismic stratigraphy of the northern sin, Rocky Mountain Association of Geologists, 1981 Field Conference, Guidebook, p. 147–159. Uncompahgre front, Grand County, Utah, in Lowell, J.D., and Gries, R., eds., Rocky Mountain Hite, R.J., Cater, F.W., and Liming, J.A., 1972, Pennsylvanian rocks and salt anticlines, Paradox Ba- Foreland Basins and Uplifts: Rocky Mountain Association of Geologists, p. 201–211. sin, Utah and Colorado, in Mallory, W.W., ed., Geologic Atlas of the Rocky Mountain Region: Fryberger, S.G., Schenk, C.J., and Krystinik, L.F., 1988, Stokes surfaces and the effects of near-sur- Rocky Mountain Association of Geologists, p. 133–138. face groundwater-table on aeolian deposition: Sedimentology, v. 35, p. 21–41, doi:10.1111 /j Hoy, R.G., 2000, Syndepositional deformation, sedimentation, and regional tectonics of an Ances- .1365-3091.1988.tb00903.x. tral Rocky Mountains basin, Central Colorado trough, Colorado [Ph.D. thesis]: West Lafayette, Gehrels, G.E., 2012, Detrital zircon U-Pb geochronology: Current methods and new opportunities, Indiana, Purdue University, 252 p. in Busby, C., and Azor, A., eds., Tectonics of Sedimentary Basins: Recent Advances: Oxford, Hoy, R.G., and Ridgway, K.D., 2002, Syndepositional thrust-related deformation and sedimen- UK, Wiley-Blackwell, p. 47–62. tation in an Ancestral Rocky Mountains basin, Central Colorado trough, Colorado, USA:

Geological Society of America Bulletin, v. 114, p. 804–828, doi:10.1130/0016-7606(2002)114 Lawton, T.F., Hunt, G.J., and Gehrels, G.E., 2010, Detrital zircon record of thrust belt unroofing in <0804:STRDAS>2.0.CO;2. Lower Cretaceous synorogenic conglomerates, central Utah: Geology, v. 38, p. 463–466, doi: Hunter, R.E., 1977, Basic types of stratification in small eolian dunes: Sedimentology, v. 24, 10.1130/G30684.1. p. 361–387, doi:10.1111/j.1365-3091.1977.tb00128.x. Lindsey, D.A., Johnson, B.J., and Andriessen, P.A.M., 1983, Laramide and Neogene structure of Huntoon, J.E., and Chan, M.A., 1987, Marine origin of paleotopographic relief on eolian White the Sangre de Cristo Range, south-central Colorado, in Lowell, J.D., and Gries, R., eds., Rocky Rim Sandstone (Permian), Elaterite Basin, Utah: The American Association of Petroleum Mountain Foreland Basins and Uplifts: Rocky Mountain Association of Geologists, p. 219–228. Geologists Bulletin, v. 71, p. 1035–1045. Loope, D.B., 1984, Eolian origin of upper Paleozoic sandstones, southeastern Utah: Journal of Huntoon, J.E., Dubiel, R.F., Stanesco, J.D., Mickleson, D.L., and Condon, S.M., 2002, Permian- Sedimentary Petrology, v. 54, p. 563–580. Triassic depositional systems, paleogeography, paleoclimate, and hydrocarbon resources in Mack, G.H., and Rasmussen, K.A., 1984, Alluvial fan sedimentation of the Cutler Group (Permo- Canyonlands and Monument Valley, Utah: Geological Society of America Field Guides, v. 3, Pennsylvanian) near Gateway, Colorado: Geological Society of America Bulletin, v. 95, p. 33–58; doi: 10.1130/0-8137-0003-5.33. p. 109–116, doi:10.1130/0016-7606(1984)95<109:ASOTCF>2.0.CO;2. Ingersoll, R.V., Bullard, T.F., Ford, R.L., Grimm, J.P., Pickle, J.D., and Sares, S.W., 1984, The effect Mallory, W.W., 1972a, Pennsylvanian arkose and the Ancestral Rocky Mountains, in Mallory, W.W., of grain size on detrital modes: a test of the Gazzi-Dickinson point-counting method: Journal ed., Geologic Atlas of the Rocky Mountain region: Rocky Mountain Association of Geologists, of Sedimentary Petrology, v. 54, p. 103–116. p. 131–132. Ingersoll, R.V., Graham, S.A., and Dickinson, W.R., 1995, Remnant ocean basins, in Busby, C.J., Mallory, W.W., 1972b, Pennsylvanian System: Regional synthesis, in Mallory, W.W., ed., Geologic and Ingersoll, R.V., eds., Tectonics of Sedimentary Basins: Cambridge, Blackwell, p. 363–391. Atlas of the Rocky Mountain Region: Rocky Mountain Association of Geologists, p. 111–128. Irwin, C.D., 1971, Stratigraphic analysis of Upper Permian and Lower Triassic strata in southern Marzolf, J.E., 1988, Controls on late Paleozoic and early Mesozoic eolian deposition of the western Utah: The American Association of Petroleum Geologists Bulletin, v. 55, p. 1976–2007. United States: Sedimentary Geology, v. 56, p. 167–191, doi:10.1016/0037-0738(88)90053-X. Jackson, M.P.A., and Cramez, C., 1989, Seismic recognition of salt welds in salt tectonic regimes: Matthews, W.J., Hampson, B.D., Trudgill, B.D., and Underhill, J.R., 2004, Impact of salt movement Society of Economic Mineralogists and Paleontologists, Gulf Coast Section, 10th Annual Re- on fluvio-lacustrine stratigraphy and facies architecture: Late Triassic Chinle Formation, north- search Conference, Program and Extended Abstracts, p. 66–71. ern Paradox Basin, SE Utah, U.S.A., in Post, P.J., et al., eds., Salt-Sediment Interactions and Jessup, M.J., Jones, J.V.I., Karlstrom, K.E., Williams, M.L., Connelly, J.N., and Heizler, M.T., 2006, Hydrocarbon Prospectivity: Proceedings, Gulf Coast Section SEPM Foundation, Annual Bob F. Three Proterozoic orogenic episodes and an intervening exhumation event in the Black Can- Perkins Research Conference (CD-ROM), v. 24, p. 931–964. yon of the Gunnison region, Colorado: The Journal of Geology, v. 114, p. 555–576, doi:10 Matthews, W.J., Hampson, G.J., Trudgill, B.D., and Underhill, J.R., 2007, Controls on fluvio .1086/506160. lacustrine reservoir distribution and architecture in passive salt-diapir provinces: Insights Johansen, S.J., 1988, Origins of upper Paleozoic quartzose sandstones, American southwest: from outcrop analogs: The American Association of Petroleum Geologists Bulletin, v. 91, Sedimentary Geology, v. 56, p. 153–166, doi:10.1016/0037-0738(88)90052-8. p. 1367–1403, doi:10.1306/05310706123. Jones, J.V., III, Connelly, J.N., Karlstrom, K.E., Williams, M.L., and Doe, M.F., 2009, Age, prove- Melton, F.A., 1925, The Ancestral Rocky Mountains of Colorado and New Mexico: The Journal of nance, and tectonic setting of Paleoproterozoic quartzite successions in the southwestern Geology, v. 33, p. 84–89, doi:10.1086 /623171 . United States: Geological Society of America Bulletin, v. 121, p. 247–264, doi:10.1130 /B26351 .1. Mountney, N.P., 2006, Periodic accumulation and destruction of aeolian erg sequences in the Jones, R.W., 1959, Origin of salt anticlines of Paradox Basin: The American Association of Petro- Permian Cedar Mesa Sandstone, White Canyon, southern Utah, USA: Sedimentology, v. 53, leum Geologists Bulletin, v. 43, p. 1869–1895. p. 789–823, doi:10.1111/j.1365-3091.2006.00793.x. Kamola, D.L., and Chan, M.A., 1988, Coastal dune facies, Permian Cutler Formation (White Rim Mountney, N.P., and Jagger, A., 2004, Stratigraphic evolution of an aeolian erg margin system: Sandstone), Capitol Reef National Park area, southern Utah: Sedimentary Geology, v. 56, The Permian Cedar Mesa Sandstone, SE Utah, USA: Sedimentology, v. 51, p. 713–743, doi: p. 341–356, doi:10.1016/0037-0738(88)90060-7. 10.1111/j.1365-3091.2004.00646.x. Keller, G.R., and Hatcher, R.D., Jr., 1999, Some comparisons of the structure and evolution of the Mueller, P.A., Heatherington, A.L., Foster, D.A., Thomas, W.A., and Wooden, J.L., 2014, The southern Appalachian-Ouachita orogen and portions of the Trans-European suture zone re- Suwannee suture: Significance for Gondwana-Laurentia terrane transfer and formation of gion: Tectonophysics, v. 314, p. 43–68. Pangaea: Gondwana Research, v. 26, p. 365–373, doi:10.1016/j.gr.2013.06.018. Kluth, C.F., 1986, Plate tectonics of the Ancestral Rocky Mountains, in Peterson, J.A., ed., Paleotec- Orgill, J.R., 1971, The Permian–Triassic unconformity and its relationship to the Moenkopi, Kai- tonics and Sedimentation in the Rocky Mountain Region, United Sates: American Association bab, and White Rim formations in and near the San Rafael Swell, Utah: Brigham Young of Petroleum Geologists Memoir 41, p. 353–369. University Research Studies: Geology Series, Part 3, v. 18, p. 131–179. Kluth, C.F., and Coney, P.J., 1981, Plate tectonics of the Ancestral Rocky Mountains: Geology, v. 9, Parr, T.R., 2012, Correlation of the Castle Valley Eolianite, Castle Valley, Utah, and the influence of p. 10–15, doi:10.1130/0091-7613(1981)9<10:PTOTAR>2.0.CO;2. the Castle Valley salt diapir on depositional setting and stratigraphic geometry [M.S. thesis]: Kluth, C.F., and DuChene, H.R., 2009, Late Pennsylvanian and Early Permian structural geology Las Cruces, New Mexico State University, 125 p. and tectonic history of the Paradox Basin and Uncompahgre uplift, Colorado and Utah, in Parrish, J.T., and Peterson, F., 1988, Wind directions predicted from global circulation models and Houston, W.S., Wray, L.L., and Moreland, P.G., eds., The Paradox Basin Revisited—New De- wind directions determined from eolian sandstones of the western United States—A com- velopments in Petroleum Systems and Basin Analysis: Rocky Mountain Association of Geolo- parison: Sedimentary Geology, v. 56, p. 261–282, doi:10.1016/0037-0738(88)90056-5. gists, Special Paper (CD-ROM), p. 178–197. Peterson, F., 1988, Pennsylvanian to Jurassic eolian transportation systems in the western United Kwon, S., and Mitra, G., 2004, Strain distribution, strain history, and kinematic evolution asso- States: Sedimentary Geology, v. 56, p. 207–260, doi:10.1016/0037-0738(88)90055-3. ciated with the formation of arcuate salients in fold-thrust belts: The example of the Provo Rasmussen, D.L., 2009, Road logs across the Uncompahgre uplift and the deep fold and fault salient, Sevier orogen, Utah, in Sussman, A.J., and Weil, A.B., eds., Orogenic Curvature: Inte- belt, northern Paradox Basin, Colorado and Utah, in Houston, W.S., Wray, L.L., and Moreland, grating Paleomagnetic and Structural Analyses: Geological Society of America Special Paper P.G., eds., The Paradox Basin Revisited—New Developments in Petroleum Systems and Basin 383, p. 205–223. Analysis, Rocky Mountain Association of Geologists, Special Paper (CD-ROM), p. 691–778. Langford, R.P., and Chan, M.A., 1988, Flood surfaces and deflation surfaces within the Cutler Rasmussen, D.L., 2014, Namakiers in Triassic and Permian formations in the Paradox Basin (USA) Formation and Cedar Mesa Sandstone (Permian), southeastern Utah: Geological Society with comparisons to modern examples in the Zagros Fold Belt, Iran, in MacLean, J.S., Biek, of America Bulletin, v. 100, p. 1541–1549, doi:10.1130/0016-7606(1988)100<1541:FSADSW>2 R.F., and Huntoon, J.E., eds., Geology of Utah’s Far South: Utah Geological Association Publi- .3.CO;2. cation 43 (CD-ROM), p. 689–756. Langford, R.P., and Chan, M.A., 1989, Fluvial-aeolian interactions: Part II, Ancient systems: Sedi- Richards, B.C., 2013, Current status of the International Carboniferous Time Scale, in Lucas, S.G., mentology, v. 36, p. 1037–1051, doi:10.1111/j.1365-3091.1989.tb01541.x. ed., The Carboniferous–Permian Transition: Albuquerque, New Mexico Museum of Natural Lawton, T.F., and Buck, B.J., 2006, Implications of diapir-derived detritus and gypsic paleosols History and Science Bulletin 60, p. 348–353. in Lower Triassic strata near the Castle Valley salt wall, Paradox Basin, Utah: Geology, v. 34, Rowan, M.G., Lawton, T.F., Giles, K.A., and Ratliffe, R.A., 2003, Near-salt deformation in La Popa p. 885–888, doi:10.1130/G22574.1. basin, Mexico, and the northern Gulf of Mexico: A general model for passive diapirism:

The American Association of Petroleum Geologists Bulletin, v. 87, p. 733–756, doi:10.1306 Tewksbury, B.J., 1989, Proterozoic geology of the Needle Mountains; a summary, in Grambling, /01150302012. J.A., and Tewksbury, B.J., eds., Proterozoic Geology of the Southern Rocky Mountains: Geo- Schultz, A.W., 1984, Subaerial debris-flow deposition in the Upper Paleozoic Cutler Formation, logical Society of America Special Paper 235, p. 65–73. western Colorado: Journal of Sedimentary Petrology, v. 54, p. 759–772. Thomas, W.A., 2007, Pennsylvanian sinistral faults along the southwest boundary of the Un- Scotese, C.R., and McKerrow, W.S., 1990, Revised world maps and introduction, in McKerrow, compahgre uplift, Ancestral Rocky Mountains, Colorado: Geosphere, v. 3, p. 119–132, doi: W.S., and Scotese, C.R., eds., Paleozoic Paleogeography and Biogeography: Geological Soci- 10.1130/GES00068.1. ety of London Memoir 12, p. 1–21. Thomas, W.A., 2011, Detrital-zircon geochronology and sedimentary provenance: Lithosphere, Scotese, C.R., Bambach, R.K., Barton, C., Van de Voo, R., and Ziegler, A.M., 1979, Paleozoic base v. 3, p. 304–308, doi:10.1130/RF.L001.1. maps: The Journal of Geology, v. 54, p. 759–772. Thomas, W.A., 2014, A mechanism for tectonic inheritance at transform faults of the Iapetan mar- Shock, A.M., 2012, Origin and implications of Permian and Triassic diagenetic carbonate caprock gin of Laurentia: Geoscience Canada, v. 41, p. 321–344, doi:10.12789/geocanj.2014.41.048. adjacent to diapiric salt walls, Paradox Basin, Utah [M.S. thesis]: Las Cruces, New Mexico Trexler, J.H., Jr., Cashman, P.H., Snyder, W.S., and Davydov, V.I., 2004, Late Paleozoic tectonism in State University, 105 p. Nevada: Timing, kinematics, and tectonic significance: Geological Society of America Bulle- Shoemaker, E.M., and Newman, W.L., 1959, Moenkopi Formation (Triassic? and Triassic) in salt tin, v. 116, p. 525–538, doi:10.1130/B25295.1. anticline region, Colorado and Utah: The American Association of Petroleum Geologists Trudgill, B.D., 2011, Evolution of salt structures in the northern Paradox Basin: Controls on evap- Bulletin, v. 43, p. 1835–1851. orite deposition, salt wall growth and supra-salt stratigraphic architecture: Basin Research, Shoemaker, E.M., Case, J.E., and Elston, D.P., 1958, Salt anticlines of the Paradox Basin: Guide- v. 23, p. 208–238, doi:10.1111/j.1365-2117.2010.00478.x. book to the Geology of the Paradox Basin: Intermountain Association of Petroleum Geolo- Trudgill, B.D., Banbury, N., and Underhill, J., 2004, Salt evolution as a control on structural and gists, Ninth Annual Field Conference, Guidebook, p. 39–59. stratigraphic systems: Northern Paradox foreland basin, southeast Utah, USA, in Post, P.J., Silver, L.T., and Barker, F., 1968, Geochronology of Precambrian rocks of the Needle Mountains, et al., eds., Salt-Sediment Interactions and Hydrocarbon Prospectivity: Proceedings, Gulf southwestern Colorado; part 1, U-Pb results: Geological Society of America Abstracts for Coast Section SEPM Foundation (Society for Sedimentary Geology), Annual Bob F. Perkins 1967: Special Paper, v. 115, p. 204–205. Research Conference, v. 24, (CD-ROM), p. 669–700. Soreghan, G.S., and Soreghan, M.J., 2013, Tracing clastic delivery to the Permian Delaware Ba- Tucker, R.D., and Gower, C.F., 1994, A U-Pb geochronological framework for the Pinware terrane, sin, U.S.A.: Implications for paleogeography and circulation in westernmost equatorial Pan- Grenville Province, southeast Labrador: The Journal of Geology, v. 102, p. 67–78, doi:10.1086 gea: Journal of Sedimentary Research, v. 83, p. 786–802, doi:10.2110/jsr.2013.63. /629648. Soreghan, G.S., Elmore, R.D., and Lewchuk, M.T., 2002, Sedimentologic-magnetic record of Tweto, O., compiler, 1979, Geologic map of Colorado: Geological Survey of Colorado, scale western Pangean climate in upper Paleozoic loessite (lower Cutler beds, Utah): Geologi- 1:500,000, 2 sheets. cal Society of America Bulletin, v. 114, p. 1019–1035, doi:10.1130/0016-7606(2002)114<1019: Van der Plas, L., and Tobi, A.C., 1965, A chart for judging the reliability of point counting results: SMROWP>2.0.CO;2. American Journal of Science, v. 263, p. 87–90, doi:10.2475/ajs.263.1.87. Soreghan, G.S., Soreghan, M.J., Sweet, D.E., and Moore, K.D., 2009, Hot fan or cold outwash?: Van Schmus, W.R., et al., 1993, Transcontinental Proterozoic provinces, in Reed, J.C., Jr., Bickford, Hypothesized proglacial deposition in the upper Paleozoic Cutler Formation, western M.E., Houston, R.S., Link, P.K., Rankin, D.W., Sims, P.W., and Van Schmus, W.R., eds., Precam- tropical Pangea: Journal of Sedimentary Research, v. 79, p. 495–522, doi:10.2110 /jsr .2009 brian Conterminous U.S.: Boulder, Colorado, Geological Society of America, Geology of North .055. America, v. C-2, p. 171–334. Speed, R.C., and Sleep, N.H., 1982, Antler orogeny and foreland basin: A model: Geological Venus, J.H., Mountney, N.P., and McCaffrey, W.D., 2015, Syn-sedimentary salt diapirism as a con- Society of America Bulletin, v. 93, no. 9, p. 815–828, doi:10.1130 /0016 -7606(1982)93 <815: trol on fluvial-system evolution: An example from the proximal Permian Cutler Group, SE AOAFBA>2.0.CO;2. Utah, USA: Basin Research, v. 27, p. 152–182, doi:10.1111/bre.12066. Stacey, J.S., and Kramers, J.D., 1975, Approximation of terrestrial lead isotope evolution by a Ver Wiebe, W.A., 1930, Ancestral Rocky Mountains: The American Association of Petroleum two-stage model: Earth and Planetary Science Letters, v. 26, p. 207–221, doi:10.1016 /0012 Geologists Bulletin, v. 14, p. 765–788. -821X(75)90088-6. Viele, G.W., and Thomas, W.A., 1989, Tectonic synthesis of the Ouachita orogenic belt, in Hatcher, Stanesco, J.D., 1991, Sedimentology and cyclicity in the lower Permian De Chelly Sandstone on R.D., Jr., Thomas, W.A., and Viele, G.W., eds., The Appalachian-Ouachita Orogen in the United the Defiance Uplift, eastern Arizona: The Mountain Geologist, v. 28, p. 1–11. States: Geological Society of America, The Geology of North America, v. F-2, p. 695–728. Stanesco, J.D., Dubiel, R.F., and Huntoon, J.E., 2000, Depositional environments and paleotec Walker, J.D., Geissman, J.W., Bowring, S.A., and Babcock, L.E., compilers, 2012, Geologic Time tonics of the Organ Rock Formation of the Permian Cutler Group, southeastern Utah, in Scale v. 4.0: Geological Society of America, doi:10.1130/2012.CTS004R3C. Sprinkel, D.A., Chidsey, T.C., and Anderson, P.B., eds., Geology of Utah’s National Parks and Wasteneys, H.A., Kamo, S.L., Moser, D., Krogh, T.E., and Gower, C.F., 1997, U-Pb geochronological Monuments: Utah Geological Association Publication 28, p. 591–605. constraints on the geological evolution of the Pinware terrane and adjacent areas, Grenville Steele-Mallory, B.A., 1982, The depositional environment and petrology of the White Rim Sand- Province, southeast Labrador, Canada: Precambrian Research, v. 81, p. 101–128, doi:10.1016 stone Member of the Permian Cutler Formation, Canyonlands National Park, Utah: U.S. Geo- /S0301-9268(96)00030-7. logical Survey Open-File Report 82-204, 81 p. Weimer, R.J., 1980, Recurrent movement on basement faults, a tectonic style for Colorado and Stevenson, G.M., and Baars, D.L., 1986, The Paradox: A pull-apart basin of Pennsylvanian age, in adjacent areas, in Kent, H.C., and Porter, K.W., eds., Proceedings, 1980 Symposium on Colo- Peterson, J.A., ed., Paleotectonics and Sedimentation in the Rocky Mountain Region, United rado Geology: Rocky Mountain Association of Geologists, p. 23–35. States: American Association of Petroleum Geologists Memoir 41, p. 513–539. Wright, J.E., and Wyld, S.J., 2006, Gondwanan, Iapetan, Cordilleran interactions: A geodynamic Stevenson, G.M., and Wray, L.L., 2009, History of petroleum exploration of Paleozoic targets in model for the Paleozoic tectonic evolution of the North American Cordillera, in Haggart, J.W., the Paradox Basin, in Houston, W.S., Wray, L.L., and Moreland, P.G., eds., The Paradox Basin Enkin, R.J., and Monger, J.W.H., eds., Paleogeography of the North American Cordillera: Evi- Revisited—New Developments in Petroleum Systems and Basin Analysis: Rocky Mountain dence For and Against Large-Scale Displacements: Geological Association of Canada Special Association of Geologists, Special Publication (CD-ROM), p. 1–23. Paper 46, p. 377–408.