Interactions Between Axial and Transverse

Interactions between axial and transverse drainage systems in the Late Cretaceous Cordilleran foreland basin: Evidence from detrital zircons in the Straight Cliffs Formation, southern Utah, USA

Tyler S. Szwarc1, Cari L. Johnson1,†, Lisa E. Stright1, and Christopher M. McFarlane2 1Department of Geology and Geophysics, University of Utah, 115 S 1460 E, Sutton 383, Salt Lake City, Utah 84112, USA 2Department of Earth Sciences, University of New Brunswick, 2 Bailey Drive, Fredericton, NB E3B 5A3, Canada

ABSTRACT sandstones, which favor a felsic intrusive 2005; May et al., 2013), and related stratigraphic source, and (2) prominent 1.4 and 1.7 Ga architecture with variations in relative sea level New detrital zircon geochronologic data zircon populations. The 1.4 and 1.7 Ga peaks (Olsen et al., 1995; Van Wagoner, 1995), climate from the Straight Cliffs Formation of south- are the only dominant Proterozoic peaks in (Drummond et al., 1996), autogenic patterns ern Utah provide insight into the controls samples from the Straight Cliffs Formation, (Wang et al., 2011), and tectonic subsidence on stratigraphic architecture of the Western whereas samples derived more directly from associated with fold-and-thrust belt development Interior Basin during Turonian–early Cam- the Sevier fold-and-thrust belt tend to have a (Robinson and Slingerland, 1998; Horton et al., panian time. Detrital zircon ages (N = 40, broader distribution of Proterozoic age peaks. 2004; Edwards et al., 2005). n = 3650) derived from linked fl uvial and Up-section architectural trends in the Factors governing axial fl uvial architecture shallow-marine depositional systems of the Straight Cliffs Formation are linked to have remained largely unstudied in Cordi lleran Kaiparowits Plateau indicate the majority trends in detrital zircon geochronologic data, foreland strata, but new detrital zircon geo- of zircons in fl uvial strata were derived from underscoring the likelihood of common driv- chronologic data from the Turonian–Campanian the Mogollon Highlands (1.25–1.90 Ga, 67% ers and controls. The axial system depositing Straight Cliffs Formation help to elucidate the of fl uvial zircons), with subordinate contri- Straight Cliffs fl uvial strata was primarily relationship between source rocks and basin sedi- butions delivered from the Sevier fold-and- fed by drainages originating in the Mogol- menta tion. Approximately 10 m.y. of fl uvial and thrust belt (265–1250 Ma, 17%) and Cordi- lon Highlands during a pulse of tectonic alluvial deposition are preserved in the Straight lleran magmatic sources (81–265 Ma, 16%). activity in the Maria fold-and-thrust belt Cliffs Formation in the Kaiparowits Plateau of Integration of these data with fl uvial facies and generally high subsidence rates in the southern Utah (Figs. 1 and 2; Table 1), enabling distributions, petrography, clast counts, foreland basin (Turonian–Santonian). Over detailed investigation into the controls on fl u- and evidence of magmatic arc sources from time, activation of the Paxton duplex in the vial architecture. Among the challenges associ- the Mohave region of California implies the Sevier fold-and-thrust belt (early Campan- ated with linking fl uvial architecture to potential presence of a northeast-fl owing, axial fl uvial ian) exhumed proximal foreland basin strata driving factors is the diffi culty of distinguishing system. This system was fed by rivers drain- and enabled drainage systems from the Se- between axial and transverse deposition, not ing the Mogollon Highlands to the south vier fold-and-thrust belt to feed into the ba- only spatially throughout the basin, but also as and by transverse drainages from the Sevier sin more prominently. The results presented the systems evolve through time. Resolving the fold-and-thrust belt to the west. Compared here underscore the potential signifi cance of detrital zircon provenance of these Cordilleran to the fl uvial deposits, shallow-marine sand- axial fl uvial systems and their complex inter- foreland basin deposits remains a challenge stones have a greater proportion of Sevier play with transverse drainage networks in due to overlap between zircon age populations fold-and-thrust belt–derived zircons (42%), foreland basins. in the likely source areas on the basin margins. which were delivered via longshore currents However, by integrating new detrital zircon geo- from the north. Shallow-marine samples also INTRODUCTION chronological data with sandstone petrology, contain less Mogollon input (44%) compared paleocurrent measurements, and clast counts, the to contemporaneous fl uvial systems, and Modern foreland basin systems contain both ambiguity of source rock provenance signatures similar input from the magmatic arc (14%). transverse and axial rivers (generally oriented adjacent to the foreland basin can be reduced, Although Proterozoic zircons associated with orthogonal and parallel to the fold-and-thrust and axial fl uvial deposits can be more clearly the Mogollon Highlands are also present in belt, respectively) that deliver and redistribute differentiated from their transverse counterparts. the Sevier fold-and-thrust belt, several lines sediment throughout the basin. To date, most Previous studies of the Straight Cliffs Forma- of evidence argue for a distinct southerly studies of Cordilleran foreland basin architec- tion (e.g., Peterson, 1969a, 1969b; Shanley and source for the Straight Cliffs Formation. ture have focused on transverse fl uvial deposits McCabe, 1991, 1993, 1995; Hettinger, 1995, These include (1) moderate proportions of (Lawton, 1983, 1986; Fillmore, 1989, 1991; 2000; Allen and Johnson, 2010a, 2010b, 2011; feldspar and angular quartz grains in fl uvial Goldstrand, 1994; Olsen et al., 1995; Horton Gallin et al., 2010; Gooley, 2010; Dooling, et al., 2004; DeCelles et al., 1995; DeCelles and 2013; Pettinga, 2013; Fig. 3) provide a neces- †E-mail: [email protected]. Cavazza, 1999; DeCelles, 2004; Edwards et al., sary framework in which to relate controls on

GSA Bulletin; March/April 2015; v. 127; no. 3/4; p. 372–392; doi: 10.1130/B31039.1; 16 ﬁ gures; 4 tables; Data Repository item 2014310; published online 16 September 2014.

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fl uvial and marginal marine architecture to the Legend sedimentary source terranes adjacent to the Cor- dilleran foreland basin. With strong facies con- Active Thrust trol across the Kaiparowits Plateau, it is possible WY Inactive Thrust to identify variability in sediment sources and delivery within distinct stratigraphic intervals Santonian and depositional environments. Additionally, Paleoshoreline changes in provenance through time can be related to tectonic processes in both the Sevier Upper Cretaceous fold-and-thrust belt and Mogollon Highlands, Foreland Basin which heavily infl uenced the evolution of fl u- UT Deposits (present) vial systems in the Kaiparowits region of the 40° N foreland basin.

NV REGIONAL GEOLOGY

The Straight Cliffs Formation records ﬂ uvial and marginal marine deposition adjacent to sev- CNTB PX eral prominent paleogeographic features dur- PV Fig. 2 ing Turonian–early Campanian time (Fig. 1). A CR Western major source area for these depositional systems Sevier fold- Interior is presumed to be the Sevier fold-and-thrust and-thrust belt Seaway belt, a mountain chain situated at the eastern- WW most extent of the Cordilleran hinterland that 94–3000 Ma zircons KB BMT trended northeast through southern Utah (Arm- CO strong, 1968; DeCelles, 2004). Approximately 300 km south of the Kaiparowits Basin were ESTB the Mogollon Highlands, a northwest-trending CA KT topographic high in central Arizona and New Cordilleran magmatic arc Mexico that was uplifted during several tectonic AZ events throughout Mesozoic time (Bilodeau, 1986; Salem, 2009). West of these mountain 81–250 Ma zircons 35° N belts, there was the Cordilleran magmatic arc, KMM an active volcanic chain of subduction-related Mogollon highlands magmatism spanning the western margin of the North American plate (Barth and Wooden, 1250–1900 Ma zircons 2006). The eastern edge of the Kaiparowits Pla- teau was marked by the Coniacian–early Cam- panian shoreline of the Western Interior Seaway, an epicontinental sea that connected the Gulf of USA Maria fold- Mexico to Arctic Canada throughout much of and-thrust belt Late Cretaceous time (Kauffman, 1977). 0 km 400 N 111° W NM Sevier Fold-and-Thrust Belt

Figure 1. Paleoreconstruction of southwestern North America during Coniacian–Santonian Late Cretaceous subduction of the Farallon time (after DeCelles, 2004). The Kaiparowits Basin (KB) was situated between the Sevier fold- plate beneath the western margin of the North and-thrust belt to the west and the shoreline of the Western Interior Seaway to the east. The American plate induced east-west crustal short- Mogollon Highlands were located south of the Kaiparowits Plateau in central Arizona. The Cor- ening through most of present-day Nevada and dilleran magmatic arc extended from southern Arizona, through California, and continued western Utah (Burchfi el and Davis, 1972, 1975). north along the continental margin. Primary detrital zircon ages associated with each source ter- More than 300 km of shortening was accom- rane are labeled in shaded regions. Age data compiled from Chen and Moore (1982), Schermer modated by large horizontal-offset (>100 km) and Busby (1994), Gerber et al. (1995), Coleman and Glazner (1997), Ferguson et al. (2004), thrust faults in the Sevier fold-and-thrust belt Barth and Wooden (2006), Amato et al. (2008), Dickinson and Gehrels (2009), Lawton et al. (DeCelles and Coogan, 2006). The easternmost (2010), and Spencer and Pecha (2012). Present-day exposures of Upper Cretaceous foreland extent of the Sevier fold-and-thrust belt during basin fi ll are designated by light-gray shading. Abbreviations: BMT—Blue Mountain thrust; Turonian–early Campanian time was located CNTB—Central Nevada thrust belt; CR—Canyon Range thrust; ESTB—Eastern Sierra thrust ~100 km west of the Kaiparowits Plateau (Fig. 1; belt; KB—Kaiparowits Basin; KMM—Keaney/Mollusk Mine thrust; KT—Keystone thrust; Allmendinger, 1992; Burchfi el et al., 1992; PV—Pavant thrust; PX—Paxton thrust; WW—Wah Wah thrust. States: AZ—Arizona, CA— DeCelles, 2004). During this time, thin-skinned California, CO—Colorado, NM—New Mexico, NV—Nevada, UT—Utah; WY—Wyoming. deformation and erosion of the Paxton, Pavant,

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Utah Sevier Buck Hollow fold- Main and- Western Canyon Escalante thrust PaunsauguntPaPaunnsas ugunnt Interior belt PlateauPlP ateae u Seaway

Figure 2. Map of the Kaiparo- wits Plateau in southern Utah. Highway 12 Shaded regions represent 37°60′ N present-day exposures of the Straight Cliffs Formation. Black Heward Creek circles indicate locations where Left Hand detrital zircon samples, paleo- Collet currents, clast counts, and/or Fifty Mile M petrographic samples were col- KaiparowitsKaaipi arrowwitts Rogers PlateauPlata eaau Canyon lected. Heward Creek is located ountain on the eastern edge of the Paun- saugunt Plateau.

East Kaibab Monocline

Kelly 37°20′ N Rock Grade House Bull Tibbet Cove Canyon Canyon N Highway 89 Big Water 020km e Powell 112°0′ W Lak 111°0′ W

and Canyon Range thrust sheets in central Utah which formed a northwest-trending topographic ment rock in central Arizona (Wasserburg and and the Blue Mountain, Wah Wah, and Keystone high in central Arizona known as the Mogollon Lanphere, 1965; Ferguson et al., 2004; Spencer thrusts in southern Utah and Nevada (Fig. 1) Highlands (Fig. 1; Bilodeau, 1986). Northeast- and Pecha, 2012). Although the Mogollon exposed Proterozoic through Mesozoic sedi- ward tilting and uplift of early Mesozoic and Highlands remained relatively inactive through- mentary and metasedimentary units throughout Paleozoic strata adjacent to the rift basin formed out Late Cretaceous time, minor episodes of the Sevier fold-and-thrust belt (Miller, 1966; the southwestern margin to the Cor di lleran crustal shortening may have aided in the exhu- Armstrong, 1968; DeCelles and Coogan, 2006). foreland basin in northern Arizona. During mation of Proterozoic basement rocks through- Early Cretaceous time, Mesozoic and Paleozoic out the region (Fig. 1; e.g., the Maria fold-thrust Mogollon Highlands sedimentary rocks exposed in the Mogollon belt; Knapp and Heizler, 1990; Spencer and Highlands were eroded and transported south- Reynolds, 1990; Salem, 2009). Regional corre- In addition to the Sevier fold-and-thrust west into the Bisbee and McCoy Basins and lations of Cordilleran foreland basin strata docu- belt, topography was present along the south- northeast into the Cordilleran foreland basin ment signiﬁ cant unconformities beneath Upper ern margin of the Cordilleran foreland basin in (Bilodeau and Lindberg, 1983; Bilodeau, 1986). Cretaceous strata in Arizona and Utah, further the Mogollon Highlands. Initial uplift of the Prolonged exhumation of this relict rift shoul- implying that the Mogollon Highlands persisted region was triggered by Early Cretaceous rift- der through Late Cretaceous time resulted in the as a topographic high into Late Cretaceous time ing in southeastern Arizona and New Mexico, exposure of 1.3–1.9 Ga Yavapai-Mazatzal base- (Hayes, 1970; Peterson and Kirk, 1977).

TABLE 1. DETRITAL ZIRCON SAMPLE FACIES AND LOCATIONS Facies Heward Creek Bull Canyon Tibbet Canyon Kelly Grade Left Hand Collet Buck Hollow Total Fluvial 4 (10%) 5 (13%) 2 (5%) 2 (5%) 4 (10%) 17 (42%) Tidal 2 (5%) 1 (3%) 5 (13%) 1 (3%) 9 (23%) Marine 1 (3%) 1 (3%) 7 (18%) 5 (13%) 14 (35%) Interval DTM 1 (3%) 1 (3%) 1 (3%) 3 (8%) JHM 3 (8%) 4 (10%) 1 (3%) 5 (13%) 5 (13%) 5 (13%) 23 (57%) Calico 1 (3%) 1 (3%) 1 (3%) 1 (3%) 2 (5%) 6 (15%) SHM 1 (3%) 1 (3%) 1 (3%) 1 (3%) 4 (10%) TCM 1 (3%) 1 (3%) 1 (3%) 1 (3%) 4 (10%) Total 4 (10%) 8 (20%) 1 (3%) 8 (20%) 9 (23%) 10 (25%) Note: Numbers indicate quantity of samples collected. Abbreviations: TCM—Tibbet Canyon Member; SHM—Smoky Hollow Member; JHM—John; Henry Member; DTM—Drip Tank Member.

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Rock House Cove Bull Canyon Kelly Grade Left Hand Collet Rogers Canyon (Gooley, 2010) (Pettinga, 2013) (Gallin et al., 2010) (Dooling, 2013) (Peterson, 1969b; Age A Allen and Johnson, 2010b) (Ma) DTM Camp. A′ Alvey Coal Z. 83.6 G Rees Coal Zone F ProgradationAggradation / E Re JHM trogradation D Santonian Christensen Coal Zone C 86.3 B A Con. Progradation

89.8 SHM

Tur. TCM 50 m 10 km

Isolated fluvial channels

Fluvial channel belt Kaiparowits Shoreface Braided fluvial Plateau Vertically amalgamated Paralic fluvial channel belts A′ Coastal plain / alluvial Inclined heterolithic strata Offshore / tidally influenced fluvial

A 20 km Coal mire

Figure 3. Schematic cross section of the Straight Cliffs Formation through several study areas across the Kaiparowits Plateau (see inset and Fig. 2). Spatial and temporal variations in ﬂ uvial, tidal, and shallow-marine architecture are represented by changes in the degree of channel amalgamation, shoreline trajectory, and distribution of paralic facies. Time-scale divisions are from Gradstein et al. (2012). Ab- breviations: TCM—Tibbet Canyon Member; SHM—Smoky Hollow Member; JHM—John Henry Member; DTM—Drip Tank Member. Letters A–G refer to shorefaces of Peterson (1969a). Tur.—Turonian; Con.—Coniacian; Camp.—Campanian.

Cordilleran Magmatic Arc Straight Cliffs Formation Canyon Member marks a transition from offshore mudstone and limestone deposition to Subduction-related magmatism along the The Straight Cliffs Formation is well exposed sandstone and siltstone deposition in the Kai- Cordilleran magmatic arc between roughly 260 throughout the Kaiparowits Plateau, located in parowits Basin of south-central Utah. Shanley and 81 Ma (Chen and Moore, 1982; Miller et al., the Grand Staircase–Escalante National Monu- and McCabe (1991) interpreted fl uvial incision 1995; Barth and Wooden, 2006) led to the devel- ment of south-central Utah (Fig. 2). Approxi- at the top of the Tibbet Canyon Member to mark opment of an additional topographic high along mately 300–500 m of Turonian–Campanian a sequence stratigraphic boundary. the western margin of the North American plate siliciclastic sedimentary deposits are exposed The Smoky Hollow Member (Fig. 3) is com- (Fig. 1). Triassic through Cretaceous volcanic throughout the Kaiparowits Plateau, providing posed primarily of ~20–30 m of isolated fl uvial and plutonic detritus from southern California, a nearly complete record of the marginal marine sandstone bodies interbedded with carbona- Arizona, and central Nevada was likely carried environment present during the initial retreat ceous fl oodplain mudstones and thin coal seams by a network of drainages fl owing eastward of the Western Interior Seaway. The earliest (Peterson, 1969b). These fi ne- to coarse-grained into the Cordilleran foreland basin (Dickinson stratigraphic correlations of the Straight Cliffs terrestrial deposits represent a basinward shift and Gehrels, 2009). Three primary pulses of Formation were performed by Peterson (1969a, of facies, perhaps resulting from a regional subduction-related magmatism occurred in the 1969b). In doing so, he subdivided the forma- drop in base level (Bobb, 1991; Shanley and Cordilleran magmatic arc during Mesozoic time tion into the Tibbet Canyon (TCM), Smoky McCabe, 1991). The top of the Smoky Hol- (225–200 Ma, 186–144 Ma, and 125–88 Ma; Hollow (SHM), John Henry (JHM), and Drip low Member is commonly distinguished by the Bateman, 1983), but episodes of localized mag- Tank Members (DTM; Fig. 3). presence of a coarse-grained, white and orange, matism also took place within the arc (e.g., in The lowermost Tibbet Canyon Member braided fl uvial sandstone interval known as the the Mojave region of southern California around (Fig. 3) consists of ~20 m of mainly shoreface Calico bed. This regionally extensive gravel ca. 147 Ma; Schermer and Busby, 1994; Gerber strata deposited along the margin of the Western sheet is composed of laterally and vertically et al., 1995; Walker et al., 2002). Interior Seaway (Peterson, 1969b). The Tibbet amalga mated fl uvial deposits, and it records

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deposition during a period of decreased accom- Little, 1997). Subsequent studies documented series 193 nm excimer laser equipped with an modation relative to sediment supply (Bobb, trends in average channel widths, grain size, S-155 two-volume Laurin Technic Pty ablation 1991). Shanley and McCabe (1991) proposed sandstone:shale ratio, channel clustering, chan- cell. The two-volume low-volume cell ensures a sequence stratigraphic boundary at the base nel stacking, and paleofl ow direction through- identical ablation anywhere within the cell as of the Calico bed, where a regionally exten- out the Kaiparowits Plateau (Fig. 3; e.g., Gallin well as fast-washout of the ablated aerosol. The sive, erosive contact marks a drop in relative et al., 2010; Gooley, 2010; Johnson et al., 2011, laser was connected to an Agilent 7700x quadru- sea level. 2013; Pettinga, 2013). Fluvial strata near the pole ICP-MS via 4 mm nylon tubing, with a The John Henry Member is the thickest base of the Straight Cliffs Formation (Smoky Laurin Technic Pty “Squid” smoothing device (200–500 m) and most laterally variable of the Hollow Member and lower John Henry Mem- connected in-line just before the ICP-MS. Stan- four members (Fig. 3). The base of the John ber) indicate northeast-directed paleofl ow and dards and unknowns were loaded together, and Henry Member is marked by a landward shift show an up-section decrease in average grain the cell was prepared for ablation by repeated in facies recording a transgression that occurred size with a reduction in channel widths, lat- evacuation and backfi lling with high-purity He. after deposition of the Smoky Hollow Mem- eral and vertical channel amalgamation, and A typical ablation sequence consisted of at least ber. In the southern and western Kaiparowits sandstone:shale ratio. The middle John Henry 120 detrital zircons interspersed with 15 pri- Plateau, the John Henry Member consists pri- Member consists of laterally restricted chan- mary standards (1065 Ma zircon 91500), up to marily of multistory and single-story fl uvial nel belts with abundant coals and fl oodplain fi ve consistency standards (e.g., 416 Ma Temora channel belts interbedded with carbonaceous mudstones. The upper John Henry Member and zircon), as well as four analyses of NIST610 fl oodplain mudstones and coals (Shanley and Drip Tank Member document a reversed trend glass. Ablation was conducted in a mixed He McCabe, 1991, 1993, 1995; Titus et al., 2005; of increasing grain size with wider channels, (350 mL/min) and Ar (930 mL/min) atmosphere Gooley, 2010; Pettinga, 2013). In these areas, more amalgamation of channel belts, and higher at conditions of ~4 J/cm2 fl uence, 19 or 26 µm basal John Henry Member strata contain evi- sandstone:shale ratio (Gallin et al., 2010). The crater diameter (depending on grain size of dence for tidally infl uenced deposition, includ- capping strata in the Drip Tank Member consist detrital zircon population), 4.5 Hz repetition rate, ing inclined heterolithic strata, herringbone of a braided fl uvial gravel sheet with paleocur- and 30 s ablation with 25 s background. Data cross-stratification, flaser and wavy-bedded rent indicators showing mainly east-directed were reduced offl ine using Iolite v2.31 (Paton sandstones, and brackish-water ichnofossils fl ow (Lawton et al., 2014). et al., 2011) and VizualAge (Petrus and Kamber, such as Teredolites and Gastrochaenolites 2012), and data were plotted using Isoplot v3.75 (Shanley et al., 1992; Hettinger, 1995; Gallin METHODS (Ludwig, 2012). With the exception of young et al., 2010). Easternmost exposures of the John grains (younger than 500 Ma), ages more than Henry Member consist of offshore through This study focuses on detrital zircon U-Pb 5% discordant were rejected. Analyses yield- intertidal facies, and these represent the latest geochronologic data from 40 sandstone samples ing anomalously high concentrations of U and episode of Western Interior Seaway deposition collected from fi ve locations in southern Utah depleted concentrations of Th were discarded in southern Utah. Peterson (1969b) subdivided (Heward Creek, Bull Canyon, Kelly Grade, because these grains can be highly susceptible to marine exposures of the John Henry Member Left Hand Collet, and Buck Hollow; Figs. 2 Pb loss (Dickinson and Gehrels, 2009). into seven shoreface units (A–G), which were and 4; Table 1). At each location, sandstone Zircon age distributions were compared using used by subsequent studies to document strati- samples were taken from representative facies the Kolmogorov-Smirnov (K-S) test, which graphic architecture in the eastern Kaiparowits in each of the stratigraphic members exposed assigns a p value to sample pairs based on the Plateau (Fig. 3; Allen and Johnson, 2010a, in the section. Heward Creek (in the eastern- similarity of their cumulative density functions 2010b, 2011; Johnson et al., 2011; Dooling most Paunsaugunt Plateau) and Bull Canyon (Press et al., 1986). High p values ( p > 0.05) et al., 2012). (southwestern Kaiparowits Plateau) are located indicate a statistically signifi cant likelihood The uppermost Drip Tank Member consists in western exposures of the Straight Cliffs For- that two samples may have been derived from of 30–100 m of coarse-grained fl uvial sand- mation and expose fl uvial and tidally infl uenced sources with the same zircon age distributions. stones and channel lag conglomerates (Fig. 3). channel deposits. Samples collected from Kelly Low p values ( p < 0.05) suggest the samples The Drip Tank Member gradationally overlies Grade are mainly from tidal channel deposits were sourced by statistically distinguishable the John Henry Member and records a basin- and tidal bar forms at the coastal margin. Left distributions of zircon ages. ward shift in facies. Shanley and McCabe Hand Collet and Buck Hollow are positioned Detrital zircon ages were analyzed in addition (1991) proposed a sequence boundary at at the Coniacian–early Campanian shoreline, to paleocurrent measurements, sandstone modal the base of the Drip Tank Member, but more and detrital zircon samples were derived from analyses, and clast counts derived from well- recent studies have suggested that the sequence lower-middle shoreface and tidal channel sand- studied stratigraphic intervals of the Straight boundary lies near the middle of the Drip Tank stones (Table 1). Cliffs Formation. Paleocurrent measurements Member (Lawton et al., 2003; Schellenbach, Zircons were isolated using traditional den- were obtained from trough cross-stratifi ed fl u- 2013; Lawton et al., 2014). Channel bodies in sity and magnetic methods and were mounted vial sandstones, planar cross-stratifi ed accre- the Drip Tank Member are both vertically and in 25 mm epoxy plugs. For each sample, 120 tion sets, laterally and longitudinally accreting laterally amalgamated, and fl oodplain deposits zircons were randomly selected for U-Pb geo- bar forms, ripples, and fl ute casts. Paleofl ow are rare. chronologic analysis using laser ablation– measurements were obtained using a Brunton inductively coupled plasma–mass spectrometry compass oriented along the axis of trough cross- Stratigraphic Architectural Trends (LA-ICP-MS). Analyses were conducted at the stratifi ed bed forms and in the dip direction of Previous studies investigated fl uvial strata University of New Brunswick in Fredericton, accreting foresets. Sandstone petrography sam- from the Straight Cliffs Formation to iden- New Brunswick, Canada, following the method ples were point-counted to obtain relative pro- tify possible controls on alluvial architecture described by Archibald et al. (2013). Analyses portions of monocrystalline and polycrystalline (Shanley and McCabe, 1991, 1993, 1995; were obtained using a Resonetics RESOlution™ quartz (Qm + Qp), feldspar (plagioclase [P] and

376 Geological Society of America Bulletin, v. 127, no. 3/4

potassium-feldspar [K]), and lithic fragments. A′ A′ Slides were stained for feldspars, and 500 grains Buck Hollow were identiﬁ ed using a modiﬁ ed Gazzi-Dickin- Buck Hollow son method (Ingersoll et al., 1984; Dickinson, 671 m 1985; Zuffa, 1985). TS-35 RESULTS

A Heward Paleocurrent Measurements Creek Left Paleocurrent measurements (n = 4568) and Hand accretion set measurements (n = 2040) are pre- Kaiparowits Collet TS-29 sented from fl uvial strata at Rock House Cove, Plateau Bull Canyon, and Kelly Grade, as well as tidal, estuarine, and shoreface strata at Kelly Grade 20 km Kelly and Left Hand Collet (Figs. 2 and 5). Grade TS-28 46 km N Bull Fluvial Paleocurrent Directions Canyon TS-26 Paleocurrent measurements in fl uvial strata were obtained from trough cross-stratifi ed sandstones, planar cross-stratifi cation, and ripple Bull Kelly Left Hand cross-laminated strata (Gooley, 2010). Accretion Canyon Grade Collet sets were measured from laterally and longi- 310 m 285 m 270 m TS-25 tudinally accreting bar forms. These are distin- DTM TS-1 TS-20 guished to help grossly differentiate between 38 km TS-3 different modes of bar form accretion (e.g., 25 km 63 km downstream vs. lateral accretion; McLaurin and 50 m TS-6 Steel, 2007). SEM-005 Near the base of the John Henry Member at TS-5 TS-4 Rock House Cove (n = 1577), the average SEM-004 total A paleofl ow direction trends northeast (n = 1577), JHM and accretion sets are oriented obliquely toward Heward the north (Fig. 5). Middle John Henry strata Creek SEM-002 record a shift toward southeastward fl ow, with 70 m HC-4 laterally accreting bar forms advancing south TS-24 and east. Paleocurrent data from the upper John TS-34 HC-3 TS-33 Henry Member imply fl ow resumed its north- TS-32 HC-2 TS-31 east trajectory, this time with a predominance of TS-18 TS-14 TS-10 HC-1 TS-17 TS-13 TS-9 TS-23 longitudinally accreting bar forms instead of the TS-12 lateral accretion common in lower John Henry TS-16 TS-11 TS-8 TS-22 TS-15 SHM Member strata. At Bull Canyon, paleocurrent data (n = 1869; Key TCM TS-7 Fig. 5) consist of ripple cross-lamination, trough Fluvial Coal cross-stratifi ed sandstones, planar cross-stratifi - Tidal Siltstone TS-21 cation, laterally and longitudinally accreting Marine Sandstone DZ Sample bar forms, and imbricated mud clasts (Pettinga, TS-27 2013). At the base of the John Henry Member, Figure 4. Generalized measured sections from Heward Creek, Bull Canyon, Kelly Grade, mean paleofl ow measurements are directed Left Hand Collet, and Buck Hollow. Datum is the top of the Calico bed. Detrital zircon toward the northeast and show a preference (DZ) samples are indicated by a zircon and sample name. Vertical bars along left side for downstream accretion toward the northeast. of each generalized section correspond to fl uvial (white), tidal (light gray), and marine Data from the middle John Henry Member (dark gray) environments. Abbreviations: TCM—Tibbet Canyon Member; SHM— imply paleofl ow was oriented toward the east, Smoky Hollow Member; JHM—John Henry Member; DTM—Drip Tank Member. with accretion sets primarily toward the northeast. In the Drip Tank Member, paleofl ow was directed toward the southeast, and bar forms were accreting toward the northeast. north (Gallin et al., 2010). Measurements from trends, but this is likely due to the sinuous nature At Kelly Grade, fl uvial paleofl ow measure- the Drip Tank Member imply fl ow direction was of meandering fl uvial systems. However, in all ments (n = 1565; Fig. 5) in the upper John Henry oriented toward the east. Paleocurrent measure- three locations, the overall trend is consistently Member indicate paleofl ow was directed toward ments at Kelly Grade, Bull Canyon, and Rock toward the east-northeast, which is subparallel the northeast, and bar forms accreted toward the House Cove do not follow the same up-section to the Sevier thrust front at this latitude.

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Left Hand Collet Fluvial Coal Bull Canyon Kelly Grade (Dooling, 2013) Tidal Siltstone (Pettinga, 2013) (Gallin, 2010) PC AS Marine Sandstone PC AS PC AS 50° 85° Rock House Cove 105° (Gooley, 2010) 97° N = 25 N = 43 N = 127 26° 17° N = 21 355° 68° PC AS 75° 40° 49° 47° N = 41 N = 91 N = 7 N = 33 N = 1346 N = 92 66° N = 205 N = 8 89° 125° 214° N = 63 N = 174 N = 8 N = 42 84° 65° 51° 128° N = 332 N = 12 90° 167° N = 31 N = 204 N = 140 N = 420 14° 44° 113° JHM DTM 71° 112° 127° 126° 91° N = 19 N = 48 N = 249 N = 11 N = 600 N = 24 N = 91 N = 183 51° 71° 73°

22° N = 58 N = 94 138° N = 18 N = 37 107° 58°

50 m 88° N = 237 N = 12 21° 18° 21° N = 87 N = 109 66° 53° 37° 113° N = 270 N = 35 94° N = 437 N = 74 N = 44 N = 156 N = 133 N = 117

Figure 5. Paleocurrent (PC) and accretion set (AS) measurements from Rock House Cove (Gooley, 2010), Bull Canyon (Pettinga, 2013), Kelly Grade (Gallin, 2010), and Left Hand Collet (Dooling, 2013). Arrows indicate average ﬂ ow/accretion direction for each interval. Vertical bars along left side of each generalized section correspond generally to ﬂ uvial (white), tidal (light gray), and marine (dark gray) depositional environments. Abbreviations: JHM—John Henry Member; DTM—Drip Tank Member.

Tidal and Marine Paleocurrent Directions B progradational shoreface successions (Fig. 3) Allen and Johnson, 2010a, 2010b; Gallin et al., Tidal paleocurrent indicators from Kelly indicate northeastward fl ow with southeastward 2010; Gooley, 2010; Pettinga, 2013; this study). Grade (n = 929; Fig. 5) are generally oriented accretion sets. Retrogradational shoreface suc- Petrographic data from each location (Rock toward the northeast and consist of trough and cessions (C, D, E) provide evidence for south- House Cove, Bull Canyon, Kelly Grade, Left planar cross-stratifi cation, herringbone cross- eastward fl ow with accretion sets advancing to Hand Collet, and Rogers Canyon) are plotted stratifi cation, ripple cross-lamination, and both the northeast (C), southeast (D), and southwest on traditional ternary diagrams (Fig. 6). The end laterally and longitudinally accreting bar forms (E). Aggradational to progradational shoreface members on each ternary diagram represent total (Gallin et al., 2010). Tidal strata in the lower successions at the top of the John Henry Mem- quartz (Qt), feldspar (F), and unstable lithic frag- John Henry Member contain mostly unidirec- ber indicate fl ow toward the northeast (F) and ments (Lu; Dickinson, 1985). tional indicators oriented toward the north and accretion toward the east (F and G). Sandstones in the Straight Cliffs Formation accretion sets directed toward the east. Tidal are typically composed of mono- and poly- paleocurrent indicators from the middle John Sandstone Petrology crystalline quartz, potassium and plagioclase Henry Member imply that high-sinuosity and feldspar, chert, and unstable volcanic, metamor- bidirectional fl ow was directed toward the east Sandstone modal analyses were conducted for phic, and sedimentary lithic fragments. Using and west with accretion sets advancing eastward. 122 samples from all members of the Straight the relative proportions of total quartz, feldspar, Paleocurrent data from Left Hand Collet (n = Cliffs Formation across the Kaiparowits Pla- and unstable lithic fragments as a metric, Dick- 668; Fig. 5) were measured from tidally infl u- teau (Table DR1 in the GSA Data Repository1; inson (1985) subdivided the QtFLu plots into enced trough and planar cross-stratifi ed sand- seven categories representing various types of 1GSA Data Repository item 2014310, Detrital stones, ripple cross-laminations, herringbone zircon ages with raw U/Pb isotope data, is available sedimentary source terranes. Sandstone com- cross-stratifi cation, and tidal bar forms (Dooling, at http:// www .geosociety .org /pubs /ft2014 .htm or by positional data from all Straight Cliffs Forma- 2013). Measurements from the lowermost A and request to editing@ geosociety .org. tion samples plot in the recycled orogen, craton

378 Geological Society of America Bulletin, v. 127, no. 3/4

Left Hand Qt Rogers Qt Collet Canyon on Craton Crat Stratigraphic Depositional (this study) Interior (Allen and Interior Member Environment Recycl Johnson, 2010a) Recycled O

Drip Tank Transitional Orogen Transitional Marine Continental Continental rogen John Henry Tidal Smoky Hollow Dissected Arc Uplift Dissected Arc Fluvial Tibbet Canyon Transitional Arc Transitional Arc Basement Uplift Undissected Basement Undissected Arc Arc F Lu F Lu

Rock House Qt Bull Qt Kelly Qt Cove Canyon Grade (Gooley, 2010) Craton Craton Craton Interior (Pettinga, 2013; Interior (Gallin et al., 2010; Interior Recycled Orogen Recycled Orog Recycl al this study) ional this study)

nsitional ed Orogen

Tra Transitionalontinental Transit Continental C Continent

Dissected Arc Dissected Arc Uplift Dissected Arc

Transitional Arc Transitional Arc Transitional Arc Basement Basement Uplift Undissected Basement Uplift Undissected Undissected Arc Arc Arc FLuF Lu F Lu

Figure 6. Sandstone modal compositions indicating relative proportions of total quartz (Qt), feldspar (F), and unstable lithic fragments (Lu). Each point represents data from 500 grains, and the shape and shading of each point correspond to stratigraphic member and depositional environment, respectively. 1σ uncertainty for mean compositions is denoted by black polygons. Data points generally cluster within the recycled orogen, craton interior, and transitional continental categories deﬁ ned by Dickinson (1985). Fluvial samples in the John Henry Member (white diamonds) contain more feldspar than marine samples from the John Henry Member (black diamonds) and Tibbet Canyon Member (black triangles).

interior , and transitional continental provenance to polycrystalline quartz for fl uvial sandstones decreases up section through lower and middle categories (Fig. 6), implying sediment derivation averages 40, which is characteristic of interior John Henry strata, and then increases through primarily from fold-and-thrust belt and recycled cratonic sources (Dickinson, 1985). Shoreface the upper John Henry and Drip Tank Members. sedimentary sources (Dickinson, 1985). samples from the Tibbet Canyon Member (Bull In contrast, the proportion of unstable lithic Fluvial samples from the western and south- Canyon, Kelly Grade, and Left Hand Collet) grains increases through the lower and middle ern Kaiparowits Plateau (Rock House Cove, and John Henry Member (Left Hand Collet and John Henry Member and decreases through Bull Canyon, and Kelly Grade; Fig. 1) clus- Rogers Canyon; Fig. 2) cluster in the recycled the remainder of the formation. The propor- ter near the boundary between recycled oro- orogen category but generally contain more tion of feldspar remains relatively consistent gen and transitional continental, with several rounded quartz grains and smaller proportions through the John Henry Member but decreases points located in the craton interior category. of feldspar than fl uvial samples, implying recy- in the Drip Tank Member. At Left Hand Collet This distribution implies recycled sedimentary cled sedimentary rocks were a more signifi cant and Rogers Canyon, the John Henry Member strata were a likely source for these samples, as source terrane for marine strata than fl uvial records an up-section decrease in total quartz well as exposures of granitic and gneissic cra- strata (Allen and Johnson, 2010a). with an increase in unstable lithic grains. Feld- tonic rocks. The relatively high quartz content, Figure 7 shows temporal trends in sand- spar content at Left Hand Collet decreases up with subordinate amounts of feldspar and lithic stone modal compositions. Generally, samples section but remains relatively consistent at fragments, implies that magmatic arc sources document an up-section increase in total quartz Rogers Canyon. and basement block uplifts were not major from the Tibbet Canyon Member through the The up-section trends noted in fl uvial samples contributors of sediment to the foreland basin. Calico bed at the top of the Smoky Hollow indicate that cratonic and transitional continen- Sedimentary lithic fragments predominantly Member. The transition into the John Henry tal detritus is more prominent in Smoky Hollow consist of chert and sedimentary lithic frag- Member records a decrease in total quartz with and lower John Henry samples (consisting of ments, with subordinate amounts of micaceous an increase in feldspar. At Rock House Cove, abundant angular to subangular quartz and feld- material. The ratio of monocrystalline quartz Bull Canyon, and Kelly Grade, total quartz spar grains), whereas upper John Henry and Drip

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SW NE Bull Kelly Rogers Figure 7. Relative proportions of total quartz Rock House Canyon Grade Left Hand Canyon Cove (Pettinga, 2013; (Gallin et al., 2010; Collet (Allen and (Qt), feldspar (F), and unstable lithic frag- (Gooley, 2010) this study) this study) (this study) Johnson, 2010a) ments (Lu) from several stratigraphic inter- DTM vals spanning the Kaiparowits Plateau. Fluvial samples (denoted by gray back- JHM ground shading) from Rock House Cove. Bull Canyon and Kelly Grade record two JHM up-section trends in sandstone composition. JHM Calico and lower John Henry strata show an up-section decrease in total quartz with an in- Qt JHM crease in unstable lithic fragments. Feldspar F content remains relatively consistent. Upper JHM Lu John Henry and Drip Tank samples show a JHM reversed trend with increased quartz content and a decrease in feldspar and unstable lithic JHM fragments. Marine samples (denoted by

Calico white background) show an up-section decrease in quartz and an increase in unstable TCM lithic fragments. Abbreviations: TCM— Tibbet Canyon Member; JHM—John Henry Member; DTM—Drip Tank Member. 0% 100% 0% 100% 0% 100% 0% 100% 0% 100%

TABLE 2. CLAST COUNT DATA Tank strata contain an increased abundance of Chert Quartzite Sedimentary recycled orogenic detritus (well-rounded quartz Nn(%) (%) (%) grains, detrital carbonate, and chert; Fig. 7). In Calico bed 4 474 81 16 3 shoreface samples, the up-section trends are less Basal John Henry Member shoreface 4 551 56 43 1 apparent but signal a minor increase in craton- derived feldspars and lithic fragments through time. This can be attributed to an increase in fl u- Ages from all samples (N=40, n=3650) vial infl uence at the shoreline as fl uvial facies prograded eastward through time. ACBD 96 Clast Counts 1200

Clast count data (N = 8, n = 1025; Table 2) 1000

were collected from channel lag deposits in the 1680 Relative Probability Calico bed at Kelly Grade, Buck Hollow, and Main Canyon (Fig. 2). Clasts were also counted 800 from shoreface strata in the basal John Henry Member at Main Canyon. Braided ﬂ uvial strata of the Calico bed contain well-rounded pebbles Number 600 of chert (81% of clasts), quartzite (16%), and 147 sandstone (3%). These proportions are consistent 400 across the Kaiparowits Plateau and do not show any signiﬁ cant spatial trends. In comparison to 1400 225 the Calico bed, clasts from basal John Henry 200 414 1076 Member shoreface deposits show a decrease in chert (56%), with an increase in quartzite (43%), 2695 0 and a minor decrease in sandstone (1%). 0 500 1000 1500 2000 2500 3000 Age (Ma) U-Pb Geochronology Figure 8. Relative probability plot containing ages from all detrital zircons in this study Detrital zircon geochronologic data from the (N = 40 samples, n = 3650 grains). Left vertical axis corresponds to number of grains in each Straight Cliffs Formation (N = 40 samples, n = age bin (age bins span 100 m.y.). Age populations are denoted by white and gray shaded 3650 individual analyses; Table 1; Fig. 4) are bars. Population C constitutes the largest percentage of all ages from the Straight Cliffs presented using age histograms superimposed Formation (59% of all grains), followed by population B (25%), population A (13%), and on relative probability plots (Figs. 8 and 9). population D (3%).

380 Geological Society of America Bulletin, v. 127, no. 3/4

Relative Probability NE Tidal n=98 n=98 n=98 n=65 n=83 n=35 TS-23 TS-22 TS-21 TS-27 TS-26 TS-35 TS-29 TS-28 TS-25 TS-24 n=110 n=100 n=100 n=104 Fluvial Fluvial Fluvial Fluvial Fluvial 2400 2800 Shoreface Shoreface Shoreface Shoreface 2000 . Ab- ed verti- BD each sample 400 800 1200 1600 AC Distal (WIS) Tidal Tidal TS-8 TS-5 TS-7 TS-4 TS-3 TS-1 TS-9 TS-6 n=81 n=94 n=74 n=94 n=93 n=94 n=98 n=87 n=89 TS-10 Fluvial Fluvial Fluvial Shoreface Shoreface Shoreface Shoreface BD 400 800 1200 1600 2000 2400 2800 AC Tidal Tidal Tidal Tidal Tidal Tidal n=72 n=95 n=99 n=79 n=94 n=83 TS-11 TS-14 TS-13 TS-34 TS-33 TS-32 TS-31 TS-12 n=106 n=105 Fluvial Shoreface Age (Ma) BD 400 800 1200 1600 2000 2400 2800 AC Tidal n=93 n=99 n=77 n=95 n=82 n=92 n=98 TS-17 TS-16 TS-18 TS-15 n=102 TS-20 Fluvial Fluvial Fluvial Fluvial Fluvial Fluvial SEM-004 SEM-002 SEM-005 Shoreface Bull Canyon Kelly Grade Left Hand Collet Buck Hollow BD 400 800 1200 1600 2000 2400 2800 AC n=98 HC-3 HC-2 HC-1 n=86 HC-4 n=101 n=105 Fluvial Fluvial Fluvial Fluvial Proximal (SFTB) C Figure 9. Relative probability histograms for each detrital zircon sample from the Straight Cliffs Formation. Samples are group the Straight Cliffs Formation. Samples are sample from each detrital zircon histograms for 9. Relative probability Figure cally according to location and horizontally by stratigraphic interval. The name, facies, and number of grains corresponding to of grains corresponding The name, facies, and number cally according to location and horizontally by stratigraphic interval. are labeled. Background shading designates age populations A (81–265 Ma), B (265–1250 C (1.25–1.90 Ga), and D (1.9–3.0 Ga) A shading designates age populations labeled. Background are breviations: SFTB—Sevier fold-and-thrust belt; WIS—Western Interior Seaway; TCM—Tibbet Canyon Member; SHM—Smoky Hollow TCM—Tibbet Seaway; Interior WIS—Western fold-and-thrust belt; SFTB—Sevier breviations: Member. Tank Member; JHM—John Henry DTM—Drip Heward Creek BD

0 400 800 1200 1600 2000 2400 2800 C H aioJMDTM JHM Calico SHM TCM SW

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Data are also presented in Table 3, Table 4, and TABLE 3. DETRITAL ZIRCON AGES IN EACH POPULATION Table DR2 in the GSA Data Repository (see A B C D Sample name Location Interval Facies n (%) (%) (%) (%) footnote 1). Fluvial detrital zircon samples (N = HC-4 Heward Creek M JHM Fluvial 86 8 14 72 6 19) were predominantly taken from the John HC-3 Heward Creek L JHM Fluvial 101 11 9 78 2 Henry Member at Bull Canyon and Heward HC-2 Heward Creek L JHM Fluvial 98 12 15 69 3 HC-1 Heward Creek Calico Fluvial 105 11 12 76 1 Creek (Fig. 2). Additional fl uvial samples were TS-20 Bull Canyon DTM Fluvial 98 27 19 53 1 collected from the Smoky Hollow and Drip Tank SEM-005 Bull Canyon M JHM Fluvial 109 8 22 68 2 Members at Bull Canyon, Left Hand Collet, and SEM-004 Bull Canyon L JHM Fluvial 99 13 4 81 2 SEM-002 Bull Canyon L JHM Fluvial 77 9 22 68 1 Buck Hollow. Tidal samples (N = 11) were col- TS-18 Bull Canyon L JHM Tidal 94 3 27 69 1 lected from the John Henry Member at Bull TS-17 Bull Canyon Calico Fluvial 93 10 13 77 0 Canyon, Kelly Grade, and Buck Hollow. Shore- TS-16 Bull Canyon SHM Fluvial 102 23 11 64 3 TS-15 Bull Canyon TCM Marine 82 6 37 55 2 face samples (N = 10) were obtained from the TS-30 Tibbet Canyon L JHM Tidal 89 7 18 75 0 John Henry Member at Left Hand Collet and TS-34 Kelly Grade M JHM Tidal 105 12 17 69 2 TS-33 Kelly Grade L JHM Tidal 99 4 20 75 1 Buck Hollow. Additionally, shoreface samples TS-32 Kelly Grade L JHM Tidal 79 6 35 57 1 were collected from the Tibbet Canyon Mem- TS-31 Kelly Grade L JHM Tidal 94 14 19 66 1 ber at Bull Canyon, Kelly Grade, Left Hand TS-14 Kelly Grade L JHM Tidal 99 10 33 52 4 TS-13 Kelly Grade Calico Fluvial 95 20 27 52 1 Collet, and Buck Hollow. Detrital age spectra TS-12 Kelly Grade SHM Fluvial 83 5 42 53 0 have been subdivided into four age populations TS-11 Kelly Grade TCM Marine 72 1 31 63 6 (A–D). Each population may be linked with one TS-1 Left Hand Collet DTM Fluvial 101 24 28 45 4 TS-3 Left Hand Collet JHM “G” Marine 96 18 29 50 3 or more potential source regions exposed near TS-6 Left Hand Collet JHM “F” Marine 89 19 34 40 7 the Cordilleran foreland basin during Turonian– TS-5 Left Hand Collet JHM “E” Marine 94 13 37 44 6 TS-4 Left Hand Collet JHM “D” Marine 94 18 39 36 6 Campanian time. The characteristics of each age TS-10 Left Hand Collet JHM “A” Marine 93 4 45 42 9 population are outlined in this section, followed TS-9 Left Hand Collet Calico Fluvial 88 10 7 80 3 by a discussion of spatial and temporal trends TS-8 Left Hand Collet SHM Marine 81 9 22 64 5 TS-7 Left Hand Collet TCM Marine 74 4 39 57 0 observed in the data set. TS-35 Buck Hollow DTM Fluvial 100 25 27 47 1 TS-29 Buck Hollow U JHM Marine 110 14 51 30 5 Population A: Mesozoic Ages (81–265 Ma) TS-28 Buck Hollow M JHM Tidal 83 4 11 84 1 TS-26 Buck Hollow M JHM Marine 100 17 36 38 9 Mesozoic ages account for 13% of all Straight TS-25 Buck Hollow L JHM Marine 104 43 31 17 9 Cliffs ages (Fig. 8) and have major peaks at TS-24 Buck Hollow L JHM Marine 35 9 40 46 6 TS-23 Buck Hollow Calico Fluvial 88 14 18 68 0 96 Ma, 147 Ma, and 225 Ma. Mesozoic ages are TS-22 Buck Hollow Calico Fluvial 98 27 15 58 0 present in all samples and range from 1% of ages TS-21 Buck Hollow SHM Fluvial 98 19 14 63 3 in marine strata at Kelly Grade (TS-11, Tibbet TS-27 Buck Hollow TCM Marine 65 8 40 52 0 Canyon Member; Fig. 9) to 43% of ages in fl uvial Note: Abbreviations: TCM—Tibbet Canyon Member; SHM—Smoky Hollow Member; L JHM—Lower John Henry Member; M JHM—Middle John Henry Member; U JHM—Upper John Henry Member; DTM—Drip Tank strata at Buck Hollow (TS-25, John Henry Mem- Member. ber; Fig. 9). Late Paleozoic ages (250–265 Ma) commonly accompany the Mesozoic distribution and have been included in population A. proximal foreland basin deposits and wedge-top high concentrations of uranium and depleted Population A zircons originated within vol- basins (e.g., Iron Springs Formation) that were concentrations of thorium were discarded to canic and plutonic sources in the Cordilleran uplifted and exhumed during episodes of thrust eliminate ages impacted by Pb loss (Dickinson magmatic arc of southwestern Arizona and south- belt propagation (Goldstrand, 1994). Mesozoic and Gehrels , 2009). The resultant maximum ern California (Fig. 1), which was active between foreland basin strata containing arc-derived zir- depositional ages with 95% confi dence for each ca. 81 and 260 Ma (Chen and Moore, 1982; cons are a likely source for the 225 Ma age peak member are 94.3 ± 1.4 Ma (top Tibbet Canyon Miller et al., 1995; Barth and Wooden, 2006). (Dickinson and Gehrels, 2009). Member), 89.1 ± 6.3 Ma (top Smoky Hollow Turonian–Campanian zircons compose only 7% Juvenile zircons from each member show a Member), 82.8 ± 4.1 Ma (top John Henry Mem- of the total Mesozoic arc-derived population. systematic up-section decrease in the youngest ber), and 81.2 ± 2.5 Ma (lower Drip Tank Mem- The majority of Mesozoic zircons originating ages present (Fig. 10). The youngest concor- ber; Fig. 10). In general, these ages are consistent from the magmatic arc defi ne 96 Ma, 147 Ma, dant ages from each interval that overlap at 2σ with previous biostratigraphic estimates, which and 225 Ma peaks, indicating many of these arc- can be used to estimate the maximum deposi- place the Tibbet–Smoky Hollow contact roughly derived zircons were remobilized and reworked tional age of the corresponding interval. The in the Turonian Stage (index fossil Prionocyclus prior to deposition in the Kaiparowits Basin. method described by Dickinson and Gehrels hyatti), and the John Henry–Drip Tank contact in Latest Jurassic ages composing the 147 Ma peak (2009) recommends using at least three grains late Santonian–earliest Campanian time (Endo- were likely derived from 147 Ma intrusions in to obtain a robust maximum depositional age for costea baltica and Sphenoceramus patootensi- the Mojave Desert region of southern California a given sample. Analyses yielding anomalously formis; Peterson, 1969a; Cobban et al., 2000). (Schermer and Busby, 1994; Gerber et al., 1995; Walker et al., 2002), and the Late Cretaceous ages forming the 96 Ma peak were originally derived TABLE 4. MEANS AND STANDARD DEVIATIONS FOR EACH AGE POPULATION from the Sierra Nevada batholith (Coleman and A (%) B (%) C (%) D (%) Marine 10 ± 6 40 ± 5 45 ± 10 5 ± 3 Glazner, 1997). Zircons of these ages may have Tidal 9 ± 6 26 ± 10 63 ± 13 2 ± 2 been derived directly from their original mag- Fluvial 17 ± 9 17 ± 8 63 ± 16 3 ± 2 matic sources, but they may also have come from Total 13 ± 5 25 ± 12 59 ± 15 3 ± 3

382 Geological Society of America Bulletin, v. 127, no. 3/4

Youngest ages from stratigraphic intervals Error bars represent 2σ 80 82 84 Lower Drip Tank Member 86 Sant. 81.8 + 2.5 Ma John Henry Member 88 82.8 + 4.1 Ma Con.

Age (Ma) 90 92 Smoky Hollow Member Tur. Camp. 89.1 + 6.3 Ma 94 96 Tibbet Canyon Member Cen. 98 94.3 + 1.4 Ma

Figure 10. Maximum depositional ages (with 95% conﬁ dence) for each stratigraphic member in the Straight Cliffs Formation. Ages were calculated using the weighted average of the youngest three ages that overlap at 2σ, and analyses with anomalously high concentrations of uranium were discarded due to the likelihood of Pb loss. Time-scale divisions are from Gradstein et al. (2012). Cen.—Cenomanian; Tur.—Turonian; Con.—Coniacian; Sant.—Santonian; Camp.—Campanian.

Population B: Paleozoic through magmatic arc sources in eastern Laurentia and peak is centered at 1.68 Ga and contains 76% of Mesoproterozoic Ages (265–1250 Ma) Mexico (Dickinson and Gehrels, 2008b). zircons in this age population. A smaller peak Paleozoic through Mesoproterozoic ages Subordinate grains from population B may centered at 1.40 Ga represents the remaining compose 25% of all Straight Cliffs Formation have been derived from patches of sedimen- 24% of ages in this population. Compared to zircons (Fig. 8) and form a prominent Paleozoic tary cover throughout the Mogollon Highlands. one another, the relative heights of the 1.40 and peak (414 Ma) and Grenville peak (1076 Ma). Prior to the onset of Early Cretaceous rifting 1.68 Ga peaks vary among various samples, but Grains from population B range from 4% of all in the Bisbee Basin, the Mogollon Highlands there is no obvious pattern relating the heights grains in isolated fl uvial channel sandstones in region consisted of relatively undeformed and of these peaks with relative positions in the Kai- the middle John Henry Member at Bull Canyon laterally extensive Paleozoic and Mesozoic parowits Plateau or specifi c time intervals in (SEM-004) to 51% of all grains in marine strata sedimentary deposits adjacent to exposures of which the samples were deposited. The 1.68 Ga of the upper John Henry Member at Buck Hol- Yavapai-Mazatzal basement rock (Bilodeau, peak is present in 95% of Straight Cliffs samples low (TS-29). 1986). During Early Cretaceous time, uplift and and is nearly absent in three shoreface samples Zircons representing population B were pri- tilting of the Bisbee rift shoulder subjected the in the John Henry Member (TS-25, TS-26, marily derived from sedimentary and metasedi- sedimentary rocks to erosion, but patches of TS-29) at Buck Hollow (Fig. 9). The 1.40 Ga mentary units within the Sevier fold-and-thrust remaining sedimentary cover blanketed parts peak is prominent in only 50% of all samples, belt (Dickinson and Gehrels, 2009; Lawton of the Mogollon Highlands during Late Creta- most of which are fl uvial sandstones. et al., 2010). The Canyon Range, Pavant, Pax- ceous time. Triassic through Early Cretaceous Detrital zircons representing population C ton, Blue Mountain, and Wah Wah thrust sheets rocks in southern Utah and Arizona (Moenkopi, (59% of all Straight Cliffs zircons) are predomi- in southern Utah (Fig. 1) exposed Proterozoic Chinle, Navajo, Morrison, Cedar Mountain, nately derived from the Mogollon Highlands through Mesozoic quartzites, sandstones, and Burro Canyon and Dakota Formations) con- in central Arizona (Fig. 1). The 1.6–1.8 Ga and carbonate rocks containing recycled zircons of tain zircons derived from the Yavapai-Mazatzal 1.4 Ga age peaks identifi ed in most Straight Cliffs Paleozoic and Precambrian age (Miller, 1963, basement rocks, Grenville and Paleozoic mag- Formation samples are correlative with Yavapai- 1966; Fillmore, 1989, 1991; Goldstrand, 1994; matic bodies exposed in eastern Laurentia Mazatzal basement rocks in central Arizona Dickinson and Gehrels, 2009; Lawton et al., (Dickinson and Gehrels, 2008a, 2008b), and the (Wasserburg and Lanphere, 1965; Lanphere, 2010). Grenville ages (900–1250 Ma) are prom- Cordilleran magmatic arc (Bilodeau, 1986). 1968; Anderson and Bender, 1989; Gleason inent in many units within the thrust belt (Dick- et al., 1994; Hawkins et al., 1996; Spencer and inson and Gehrels, 2008a, 2008b, 2009; Lawton Population C: Mesoproterozoic and Pecha, 2012), as well as many sedimentary units et al., 2010; Lawton and Bradford, 2011) and Paleoproterozoic Ages (1.25–1.90 Ga) in the Sevier fold-and-thrust belt and throughout represent the recycling of Grenville orogenic Mesoproterozoic and Paleoproterozoic ages the southwestern United States (Dickinson and detritus originally derived from eastern Lauren- between 1.25 and 1.90 Ga represent 59% of all Gehrels, 2008a; Laskowski et al., 2013). The tia. Additionally, Paleozoic and Neoproterozoic detrital zircons from the Straight Cliffs Forma- original source of the 1.6–1.8 Ga zircons is an ages are common in the Sevier fold-and-thrust tion (Fig. 8). Ages in this population compose extensive metamorphosed magmatic belt that belt and were originally derived from remnant two signifi cant peaks. The more prominent age developed as a result of plate convergence during

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the Paleoproterozoic Mazatzal orogeny (Amato Hettinger, 2000; Allen and Johnson, 2010b) and of evidence indicate that recycled sedimentary et al., 2008). The expansive distribution of this redirected the rivers into lagoons or estuaries in sources in the Sevier fold-and-thrust belt were magmatic belt resulted in widespread exposures the central plateau (Gallin et al., 2010; Dooling, not supplying suffi cient quantities of feldspar of 1.6–1.8 Ga in the Mogollon Highlands. The 2013), or northward into a major north-trending to account for the amounts present in Straight 1.4 Ga intrusions present in the Mogollon High- fl uvial-deltaic system (Chentnik et al., 2014; Cliffs Formation strata. lands were emplaced during a smaller orogenic Mulhern et al., 2014). First-order sediment derivation from the event relative to the Mazatzal orogeny (Gleason The presence of an axial fl uvial system Mogollon Highlands is also supported by et al., 1994; Nyman et al., 1994; Daniel et al., upstream of the Kaiparowits Basin is supported the angular to subangular quartz grains that 2013); as a result, the distribution of these by detrital zircon data, including the presence compose most fl uvial deposits in the Straight smaller magma bodies is more localized than of 147 Ma zircons in the Straight Cliffs Forma- Cliffs Formation (Allen and Johnson, 2010a; that of the 1.6–1.8 Ga intrusions. tion (Fig. 8). This signature implies that 147 Ma Allen et al., 2012; Gooley, 2010; Pettinga, intrusions and volcanics in the Mojave region 2013). The angularity of these grains is inconsis- Population D: Paleoproterozoic and were supplying detritus to the foreland basin. tent with what would be expected from recycled Archean Ages (1.9–3.0 Ga) Because igneous rocks of this age are locally sedimentary sources within the Sevier fold-and- The remaining 3% of Straight Cliffs zircons restricted to the Mojave region (Lahren et al., thrust belt. Previous studies (Otto and Picard, are represented by the Paleoproterozoic and 1990; Schermer and Busby, 1994; Gerber et al., 1976; Picard, 1977a, 1977b; Beitler et al., 2005) Archean age population. These ages form small 1995; Walker et al., 2002), the river system in demonstrated that quartz grain morphologies peaks at 1.9 and 2.7 Ga and are most common the Kaiparowits Basin must have been fed by within potential Mesozoic source rocks tend to in tidal samples from the John Henry Member drainages originating in southern California and be of equal or greater roundness than what is at Kelly Grade and shoreface samples from Left southernmost Nevada, transporting sediment indicated by Straight Cliffs Formation petrog- Hand Collet (Fig. 9). The primary source for into the basin subparallel to the Sevier fold-and- raphy (Allen et al., 2012). Prominent Juras- these grains was Mesozoic, Paleozoic, and Pre- thrust belt. sic eolianites are composed of well-rounded cambrian units in the Sevier fold-and-thrust belt Further evidence for axial fl uvial systems spherical quartz grains that are likely present in (Fig. 1; Dickinson and Gehrels, 2009; Lawton includes the abundance of population C detrital Drip Tank samples (Lawton et al., 2003, 2014) et al., 2010). zircons (1.25–1.90 Ga) and petrographic data but are otherwise rare or absent in the rest of from Straight Cliffs Formation sandstones. the Straight Cliffs Formation. It is possible that DISCUSSION Although the source for population C zircons angular quartz grains could have been sourced can be traced to several potential regions span- from quartzites exposed in the Sevier fold-and- Results from detrital zircon geochronology, ning the basin margin (including the Mogollon thrust belt; however, due to the relatively low sandstone petrography, and paleocurrent analy- Highlands, Sevier fold-and-thrust belt, and abundance of quartzite clasts present in fl uvial ses provide evidence for sediment delivery from reworked Cretaceous foreland basin deposits ), lag deposits (16% of all clasts), it is unlikely that the Mogollon Highlands, Sevier fold-and-thrust several lines of evidence indicate that the these quartzites were major sediment sources belt, and Cordilleran magmatic arc into the Mogollon Highlands were the primary source for the Straight Cliffs Formation. Turonian–Campanian foreland basin of south- for population C zircons, and therefore that Finally, the distribution of Proterozoic zircon ern Utah (Fig. 1). Integration of these three data an axial drainage system transported sediment ages in the Sevier fold-and-thrust belt is gener- sets reduces the ambiguity associated with each northeastward into southern Utah. ally broader than what is observed in Straight provenance tool and enables source rocks with The abundance of potassium feldspar in Cliffs fl uvial strata and Mogollon Highlands similar provenance signatures to be differenti- Straight Cliffs fl uvial strata (7%–26% of all basement rock. To date, there have been no ated from one another. grains, average 18%) requires that the source reported age signatures from the Sevier fold- for these rocks contained an equal or greater and-thrust belt that contain primarily 1.4 Ga and Evidence for an Axial Drainage System percentage of feldspar. In the case of the 1.7 Ga peaks resembling those in the Straight Mogollon Highlands, the Yavapai-Mazatzal Cliffs Formation and the Mogollon Highlands. Fluvial paleocurrent measurements from basement rock is largely composed of granitic Strata that do contain these two peaks also con- the Straight Cliffs Formation show an overall and grano dioritic intrusive bodies (Amato et al., tain prominent Grenville, Paleoproterozoic, and east-northeastward orientation for rivers in the 2008) containing up to 54% feldspar (Jagger Archean peaks that are not well represented in Kaiparowits Basin. This segment of the drain- and Palache, 1905), which is greater than the Straight Cliffs fl uvial samples (Fig. 11; Dick- age system has an oblique orientation compared proportion observed in fl uvial sandstones in the inson and Gehrels, 2009; Lawton et al., 2010, to the north-northeast strike of the Sevier thrust Straight Cliffs Formation. Strata in the Sevier 2014; Laskowski et al., 2013). Several Protero- front at this latitude. However, rivers entering fold-and-thrust belt typically yield smaller zoic quartzite units in the Sevier fold-and-thrust the Kaiparowits Basin are only one small part of proportions of feldspar than what is observed belt have prominent 1.4 Ga and 1.7 Ga peaks the greater axial drainage network. It is possible in fl uvial strata of the Straight Cliffs Forma- matching those seen in the Straight Cliffs For- that these rivers were redirected from the main tion (Otto and Picard, 1976; Uygur and Picard, mation (Fig. 11; Lawton et al., 2010), but due to axial drainage orientation due to back water 1980; Allen and Johnson, 2010a; Trendell et al., the relative scarcity of quartzite clasts in fl uvial infl uences as they approached the shoreline, 2012). Other Late Cretaceous foreland basin lag deposits, it is unlikely that these quartzites which was oriented nearly perpendicular to the deposits in southern Utah (Iron Springs Forma- were the dominant source of 1.4 and 1.7 Ga zir- overall paleocurrent direction (Johnson et al., tion) and central Utah (Indianola Group, Black- cons. Although these lines of evidence do not 2013; Pettinga, 2013). The axial river system hawk Formation) that were primarily sourced exclude the Sevier fold-and-thrust belt as a sedi- was further infl uenced by raised coal mires in from the Sevier fold-and-thrust belt contain an ment source, they serve to support the Mogollon the central plateau that impeded direct outputs average of ~3% feldspar (Lawton, 1986; Gold- Highlands as the primary source for population to the shoreline (McCabe and Shanley, 1992; strand, 1992; Horton et al., 2004). These lines C zircons present in Straight Cliffs fl uvial strata.

384 Geological Society of America Bulletin, v. 127, no. 3/4

Detrital zircon ages from Sevier fold-thrust belt correlative strata the western plateau (Bull Canyon and Heward Creek; Fig. 9). Up to 35% of zircons from Left ACBDHand Collet are represented by populations B G: Lower Cretaceous fluvial sandstones and D, and individual samples include as many Cedar Mountain, Burro Canyon, Jackpile, Cintura Formations as 54% (TS-10, basal shoreface deposits in the (Dickinson and Gehrels, 2009) 440 615 1100 John Henry Member). At Buck Hollow and 1440 N=5, n=445 1700 1850 Kelly Grade, a similarly high proportion was observed, with 31% and 29% of all ages corresponding to populations B and D, respectively. 420 By comparison, populations B and D represent F: Upper Jurassic fluvial sandstones 1100 only 19% of ages at Bull Canyon and 15% at 615 Morrison Formation (Dickinson and Gehrels, 2009) Heward Creek (Fig. 9). 1480 1680 N=8, n=674 Spatial variations in detrital zircon U/Pb age distributions are linked to the transition from 420 ﬂ uvial deposition in the southern and western 1065 Kaiparowits Plateau to tidal and marine depo- E: Jurassic eolianites sition in the northern and eastern plateau (Fig. 615 (Dickinson and Gehrels, 2009) 12). The ﬂ uvial sections at Heward Creek and N=10, n=890 1455 1670 1855 Bull Canyon were primarily fed by rivers draining the Mogollon Highlands, with subordinate input from the Sevier fold-and-thrust belt and 1110 Cordilleran magmatic arc (Fig. 13). The higher 235 1440 D: Triassic fluvial sandstones proportion of population B and D zircons in 445 535 Chinle Formation (Dickinson and Gehrels, 2009) shoreface and tidal samples implies additional 1700 N=6, n=558 sediment was derived from Sevier sources and transported to the Kaiparowits Basin via long-

Relative Probability shore currents. When compared using Kol- 1440 mogorov-Smirnov (K-S) statistics (Press et al., C: Early-Middle Paleozoic quartzite 1986), the resultant p values for fl uvial-tidal, fl u- Cove Fort Quartzite 1730 vial-marine, and tidal-marine comparisons are 1110 (Lawton et al., 2010) N=1, n=84 0.002, 0.000, and 0.000, respectively. P values less than 0.05 imply that the age signatures are not similar enough to have been derived from B: Proterozoic quartzite the same source distributions. 1790 Prospect Mountain Quartzite Age signatures from the two fl uvial-domi- 1400 (Lawton et al., 2010) nated successions (Bull Canyon and Heward N=1, n=89 600 1170 Creek; Fig. 9) are similar and record only minor spatial variations in fl uvial provenance. Sam- ples near the base of the John Henry Member at 1080 Heward Creek (HC-2) and Bull Canyon (SEM- A: Proterozoic quartzite 002) yield a K-S p value of 0.898, implying a Caddy Canyon Quartzite 1400 statistically signifi cant likelihood that these (Lawton et al., 2010) zircons were derived from the same sources. 1840 N=1, n=89 Detrital zircon ages from both locations show 0 200 400 600 800 1000 1200 1400 1600 1800 2000 2200 2400 2600 2800 3000 similar proportions of each age population. At Age (Ma) Heward Creek, 74% of ages correspond with population C, 13% with population B, 11% Figure 11. Detrital zircon ages from stratigraphic units locally correlative to Sevier fold- with population A, and 2% with population D. and-thrust belt strata. Mesozoic strata contain an abundance of ages from populations A At Bull Canyon, 74% correspond with popula- (not shown), B, and D. Precambrian strata from the Canyon Range thrust sheet contain tion C, whereas 15%, 8%, and 2% correspond zircons from populations B, C, and D. Figure is modifi ed from Dickinson and Gehrels with populations B, A, and D, respectively. (2009) and Lawton et al. (2010). Temporal Provenance Trends

Spatial Provenance Trends associated with each environment. There is a Detrital zircon ages record up-section trends higher proportion of sediment derived from the that coincide with temporal variations in strati- Detrital zircon age signatures vary spa- Sevier fold-and-thrust belt (populations B and graphic architectural elements and petrologic tially across the Kaiparowits Plateau, and this D) in samples from the northern and eastern pla- data (Fig. 14). In general, temporal trends reveal is primarily linked to changes in depositional teau (Left Hand Collet, Buck Hollow, and Kelly that ﬂ uvial successions (Heward Creek and processes and sediment delivery mechanisms Grade; Fig. 9) relative to samples collected in Bull Canyon) record an up-section decrease in

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Age distributions from sedimentary facies change in the middle John Henry Member in the southwestern plateau is likely due to an increase ACBDin basin accommodation rates and, subsequently, 96 a higher preservation potential for these un stable mineralogies. The highly amalgamated and D A braided fl uvial deposits of the upper John Henry 5% 10% and Drip Tank Members show an increase in zircons derived from the Sevier fold-and-thrust belt. At Bull Canyon, the Drip Tank Member Shoreface Samples C B (TS-20) contains 53% of zircons from popula- N=10, n=818 45% 40% tion C (Fig. 9), whereas population C in the Calico bed near the base of the section (TS-17) is represented by 77% of zircons in the sample. 1681 In tidal- and marine-dominated successions (Kelly Grade, Left Hand Collet, and Buck 408 Hollow), populations A and C show up-sec- 1039 535 1404 tion increases, whereas populations B and D 2765 decrease in relative abundance. The temporal 1682 increase in Mogollon Highlands and magmatic D A arc detritus is likely due to the increase in fl uvial 2% 9% infl uence at the shoreline as fl uvial facies pro- Tidal Samples graded eastward through time. 96 B N=11, n=1011 26% C Tectonic Controls on Provenance and Stratigraphic Architecture Relative Probability 63% 147 1380 414 493 The stratigraphic architecture of the Straight 815 1071 2702 Cliffs Formation was heavily infl uenced by the interactions between the axial and transverse 96 river systems draining the Mogollon Highlands 1677 and Sevier fold-and-thrust belt. Stratigraphic D A architectural trends in Straight Cliffs Forma- 3% 17% tion strata can be tied to variations in basin sub- Fluvial Samples sidence rates, sedimentation rates, and eustatic N=19, n=1821 B sea level, which in turn infl uenced basin accom- 147 17% modation rates and the behavior of drainage sys- C tems. Generally, the Straight Cliffs Formation 63% 225 1390 can be subdivided into three stratigraphic intervals defi ned by architectural, compositional, and detrital zircon geochronologic trends. Each 1050 412 2684 interval roughly coincides with the member stratigraphy and corresponds to synchronized 0 200 400 600 800 1000 1200 1400 1600 1800 2000 2200 2400 2600 2800 3000 trends in the aforementioned variables, which Age (Ma) are driven by fl uctuations in basin accommodation and sediment supply. These trends are sum- Figure 12. Detrital zircon ages corresponding to shoreface, tidal, and fl uvial facies. marized in Figure 15. Pie charts show relative proportion of ages from each population. Fluvial ages are Fluvial provenance in the Straight Cliffs For- dominated by grains from population C (63%), with a moderate presence of popula- mation was controlled by several factors, but tion B (17%) and A (17%) zircons. Tidal samples show an increase (relative to fl uvial it appears to have been most infl uenced by the samples) in ages from population B (26%), and a decrease in population A (9%). Com- interplay between tectonically driven sediment pared to both fl uvial and tidal samples, marine samples record a more signifi cant prov- supply and foreland basin subsidence rates. In enance shift, with population B increasing (40%) and population C decreasing (45%). the Mogollon Highlands, evidence suggests that periods of tectonic activity in the Maria fold- and-thrust belt (Salem, 2009) broadly coincided Mogollon Highlands–derived sediment through tain a predominance of Mogollon Highlands– with pulses of population C zircons and coarse- the John Henry Member, with an increase in derived zircons. This provenance signature is grained quartzofeldspathic sediment into the sediment derived from the Sevier fold-and- maintained through lower and middle John Kaiparowits Basin (Fig. 15, lowermost trend). thrust belt and volcanic sources. The quartz- Henry Member strata, despite a higher propor- During late Turonian time, active thrusting in rich, highly amalgamated fl uvial deposits of the tion of feldspar and unstable lithic grains in the the Maria fold-and-thrust belt (Salem, 2009) Calico bed and lower John Henry Member con- isolated channel deposits. The compositional and related uplift in the Mogollon Highlands

386 Geological Society of America Bulletin, v. 127, no. 3/4

A Legend Active Thrust Front N Paleoshoreline

Channel Complex SFTB UT

Transverse Fan

Figure 13. Paleogeographic reconstruction of the Cordilleran fore- Raised Coal Mire WIS land basin during Santonian time. A large axial ﬂ uvial system was fed by transverse drainages emerging from the Sevier fold-and- thrust belt, but the majority of sediment feeding into the axial sys- KP tem was derived from the Mogollon Highlands and the Cordilleran magmatic arc. In the Kaiparowits Basin, backwater effects from the NV Figure 16 Western Interior Seaway and raised coal mires near the shoreline locally diverted the axial system from its northeast trajectory, ulti- mately resulting in a series of east-ﬂ owing rivers that terminated in lagoonal and estuarine settings. The location of a cross section through the Sevier fold-and-thrust belt and Kaiparowits Basin (Fig. 16) is indicated on the map. Abbreviations: CMA—Cordilleran magmatic arc; KP—Kaiparowits Plateau; MH—Mogollon Highlands; SFTB—Sevier fold-and-thrust belt; WIS—Western Interior Seaway. AZ States: AZ—Arizona, CA—California, NV—Nevada, UT—Utah. 35° N CA

CMA MH 0 km 100 113° W

SW NE Heward Bull Kelly Left Hand Buck Creek Canyon Grade Collet Hollow DTM TS-20 TS-1 TS-35

JHM TS-3 TS-29

JHM SEM-005 TS-6 TS-28 Population A 81–250 Ma Magmatic Arc JHM HC-4 SEM-004 TS-34 TS-5 TS-26 Population B TS-33 250–1250 Ma JHM HC-3 SEM-002 TS-32 TS-4 TS-25 Sevier FTB TS-31 Population C 1250–1900 Ma JHM HC-2 TS-18 TS-14 TS-10 TS-24 Mogollon TS-23 Calico HC-1 TS-17 TS-13 TS-9 TS-22

SHM TS-16 TS-12 TS-8 TS-21

TCM TS-15 TS-11 TS-7 TS-27 0% 100% 0% 100% 0% 100% 0% 100% 0% 100%

Figure 14. Relative proportions of each detrital zircon age population are plotted for each sample according to location and stratigraphic interval (population D not shown due to relatively low percentages). Fluvial samples are denoted by gray background shading. Samples generally show an up-section increase in population C from the Tibbet Canyon Member (TCM) through the Smoky Hollow Member (SHM) to the Calico bed. At Heward Creek and Bull Canyon, population C decreases through the John Henry Member (JHM) into the Drip Tank Member (DTM). Samples from Kelly Grade, Left Hand Collet, and Buck Hollow show an overall increase in population C through the John Henry Member. In general, populations B and C are inversely proportional to one another, and population A shows a gradual up-section increase. Standard deviations for each population are in Table 4. FTB—fold-and-thrust belt.

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Mogollon-Derived Sandstone Modal Accommodation Eustatic Major Thrusting Age Member Zircons Relative to Composition Sea Level Events (% Population C) (% Total Quartz) Sediment Supply Drip 30%80% 50% 100% Low High – + Tank

F lu Duplex v Paxton i a Campanian l

83.6 t

a r H

t a

a t

r a

t r

)

e n

n b

i 0 o

r M

a a l

r 2 John e (

M g

i t Thrust

l . n

Paxton l

F Henry a a

a a

l l

n l.

i u t M ( Santonian v g e 1

r i a a r 9 a l

r e 9 S l M i l n i 8 t r e ) a M

t S a t r

86.3 a

t a Coniacian Thrust Belt 89.8 Smoky Hollow Maria Fold-and- Turonian Tibbet Canyon Pavant Duplex

Figure 15. Comparison of up-section trends in detrital zircon ages, sandstone modal compositions, and basin accommodation rates with potential eustatic and tectonic drivers. Data from fl uvial strata (solid lines) and marginal marine strata (dotted lines) are presented. Trends show a weak correlation with eustatic sea-level curves but are more closely linked with activation of the Maria fold-and-thrust belt (Knapp and Heizler, 1990; Barth et al., 2004; Salem, 2009) and Paxton thrust sheet in the Sevier fold-and-thrust belt (DeCelles and Coogan, 2006). Activation of the Maria fold-and-thrust belt coincides with an infl ux of population C zircons from the Mogollon Highlands (Calico bed). Increased basin subsidence rates during deposition of the lower and middle John Henry Member were likely driven by activation of the Paxton thrust sheet, which increased crustal loading in the proximal foreland basin. The upper John Henry and Drip Tank Members were deposited when the Paxton duplex was activated, which uplifted proximal foreland basin strata and enabled rivers draining the Sevier fold-and-thrust belt to deliver more sediment into the axial fl uvial system. Time-scale divisions are from Gradstein et al. (2012).

exposed Yavapai-Mazatzal source rocks, which stabilized, fi ne-grained, isolated channels (Fig. John Henry Member) and eventually braided were subsequently eroded and transported into 15, middle trend). These high subsidence rates (Drip Tank Member; Fig. 15, uppermost trend). the foreland basin (Fig. 16). Estimates for the prevented transverse rivers draining the Sevier By middle Campanian time, fl uvial systems timing of initial thrusting in the Maria fold-and- fold-and-thrust belt from prograding eastward draining the Sevier fold-and-thrust belt pro- thrust belt (Knapp and Heizler, 1990) suggest and contributing signifi cant volumes of zircon graded basinward, displacing the axial system deformation began at ca. 90 Ma. This is consis- into the axial fl uvial system. Instead, the axial eastward (Lawton et al., 2014). tent with the rapid increase in sedimentation that fl uvial system transporting sediment northward Although the timing of thrust belt activity and occurred during deposition of the Smoky Hol- from the Mogollon Highlands continued to be accommodation development appears to coin- low Member and Calico bed. Barth et al. (2004) the dominant contributor of zircon grains into cide, other potential driving factors cannot be estimated a signifi cant reduction in Maria fold- the Kaiparowits Basin (Fig. 16). disregarded. In general, the up-section trends in and-thrust belt activity at 86 Ma, which coin- In early Campanian time, the Paxton thrust stratigraphic architecture show little convincing cides with the decrease in sediment input during sheet began to deform in duplex style (DeCelles correlation to known eustatic sea-level changes deposition of the lower John Henry Member. and Coogan, 2006); as a result, the rapid vertical (Fig. 15), implying eustasy was not a primary During Santonian time, activation of the stacking of Mesozoic strata in the Paxton thrust control on the evolution of fl uvial and marine Paxton thrust sheet (Fig. 1) in the Sevier fold- sheet began to uplift the overlying proximal stratigraphy during this time. However, eustatic and-thrust belt (DeCelles and Coogan, 2006) foreland basin strata, thereby increasing trans- excursions at the Turonian-Coniacian boundary increased foreland basin subsidence rates, verse sedimentation rates (Fig. 16). The infl ux and in early Campanian time (Hardenbol et al., which enabled the axial fl uvial system in the of sediment from the Sevier fold-and-thrust 1998; Miller et al., 2005) may have contrib- Kaiparowits Basin to transition from highly belt into the axial fl uvial system caused channel uted to the reduction in accommodation space amalgamated, coarse-grained channel belts to systems to become highly amalgamated (upper during deposition of the Calico bed and Drip

388 Geological Society of America Bulletin, v. 127, no. 3/4

A Transverse Calico Bed (Coniacian) Flow Axial Flow NW 89 Ma (Sevier) (Mogollon) SE PT KP SL

50 km 100 m

Transverse Lower JHM (Santonian) Axial Flow B Flow 86–84 Ma (Sevier) (Mogollon) PT KP SL

C Upper JHM and DTM T (Early Campanian) ran Axial Flow sverse F 84–81 Ma low (Sevier) (Mogollon) KP SL

Sevier Detritus Coal Mire Coastal Plain Strata Axial Channel Belt Complex Phanerozoic Strata Marine Strata

Figure 16. Schematic cross sections oriented perpendicular to the Sevier fold-and-thrust belt and transecting the Kai- parowits Basin (see Fig. 13 for location of cross sections). (A) During Turonian–Coniacian time, crustal shortening in the Mogollon Highlands coincided with an infl ux of coarse-grained, quartzofeldspathic detritus into the foreland basin via an axial fl uvial system fl owing northeast. The primary axial channel system was located west of the Kaiparowits Plateau (KP) and east of the transverse fans draining the Sevier fold-and-thrust belt. (B) Santonian strata of the lower John Henry Member record evidence for higher accommodation in southern Utah as the Paxton thrust sheet (PT) is activated. Continued subsidence adjacent to the Sevier fold-and-thrust belt prevented transverse drainages from advancing eastward into the basin. (C) During early Campanian time, activation of the Paxton duplex (PD) resulted in the basinward progradation of transverse fans draining the Sevier fold-and-thrust belt. The additional infl ux of sediment from the Sevier fold-and-thrust belt resulted in more intense channel belt amalgamation in the Kaiparowits Basin (upper John Henry Member [JHM] and Drip Tank Member [DTM]). SL—sea level.

Tank Member (Shanley and McCabe, 1991). panian, thus favoring tectonics as a primary the interactions between axial and transverse Additionally, the effects of climate change on driving force behind increasing sediment deliv- drainage systems in the Cordilleran foreland sedimentation rates must also be considered. ery rates. Nonetheless, the infl uence of micro- basin. The abundance of Proterozoic zir- The increase in sediment input from the Sevier climates on foreland basin sedimentation may cons (1.25–1.90 Ga, 67% of all fl uvial ages), fold-and-thrust belt during the early Campanian have evolved independently of global climatic northeast-directed paleocurrent indicators, and might imply warmer, wetter climate conditions. trends, warranting further investigation. quartzofeldspathic sandstones in fl uvial strata However, several studies indicate the Santonian- imply Yavapai-Mazatzal intrusive bodies in the Campanian climate in North America gradually CONCLUSIONS Mogollon Highlands of central Arizona were cooled through time (Wolfe and Upchurch, actively feeding river systems in the Kaiparo- 1987; Huber et al., 1995). A cooler climate Detrital zircon geochronological data from wits Basin. Phanerozoic and Grenville zircons would generally imply drier conditions through the Turonian–Campanian Straight Cliffs For- are also present in Straight Cliffs fl uvial sand- time and lower sedimentation rates in the Cam- mation of southern Utah provide insight into stones (17%) and provide evidence for addi-

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tional sediment input from the Sevier fold-and- grade further into the foreland basin, thereby C.R.M., 2013, Field relationships, petrology, age, and tectonic setting of the Ordovician West Barney’s River thrust belt in southwestern Utah. Subordinate increasing sediment input from thrust belt strata. Plutonic Suite, southern Antigonish Highlands, Nova Mesozoic zircons (16%) signal a minor infl ux These interpretations are consistent with the up- Scotia, Canada. Canadian Journal of Earth Sciences, of sediment from the Cordilleran magmatic arc section increase in Phanerozoic and Grenville v. 50, p. 727–745, doi: 10 .1139 /cjes -2012 -0158 . Armstrong, R.L., 1968, Sevier orogenic belt in Nevada and or reworked volcanic material from Mesozoic zircons and well-rounded quartz grains in the Utah. Geological Society of America Bulletin, v. 79, sedimentary rocks in the Sevier fold-and-thrust upper John Henry and Drip Tank Members. p. 429–458, doi:10 .1130 /0016 -7606 (1968)79 [429: belt and Mogollon Highlands. SOBINA]2 .0 .CO;2 . Barth, A.P., and Wooden, J.L., 2006, Timing of magmatism ACKNOWLEDGMENTS Population C zircons (1.25–1.90 Ga) in the following initial convergence at a passive margin, Straight Cliffs Formation were predominantly southwestern U.S. Cordillera, and ages of lower crustal We thank Y. Luo at the University of New Bruns- magma sources. The Journal of Geology, v. 114, derived from the Mogollon Highlands. The wick for assistance with detrital zircon geochronologic p. 231–245, doi: 10 .1086 /499573 . abundance of feldspars in fl uvial sandstones analyses. Analytical work for this project was funded Barth, A.P., Wooden, J.K., Jacobson, C.E., and Probst, K., (average 18%), angular quartz grains, and by the Rocks to Models industry consortium at the Uni- 2004, U-Pb geochronology and geochemistry of the McCoy Mountains Formation, southeastern California: prominent 1.4 Ga and 1.7 Ga age peaks are versity of Utah, supported by Chevron, ConocoPhillips, Hess, Shell, and StatOil. We thank the Bureau of Land A Cretaceous retroarc foreland basin. Geological So- ciety of America Bulletin, v. 116, p. 142–153, doi:10 consistent with fi rst-order sediment derivation Management and the Grand Staircase–Escalante Na- from Proterozoic igneous bodies in the Mogol- .1130 /B25288 .1 . tional Monument for science permits to conduct this Bateman, P.C., 1983, A summary of critical relations in the lon Highlands. Zircons of this age are present in research. Thanks go to Jeff Eaton for collecting de- central part of the Sierra Nevada batholith, California, the Sevier fold-and-thrust belt, although strata trital zircon samples and corresponding stratigraphic USA, in Roddick, J.A., ed., Circum-Pacifi c Plutonic in the thrust belt typically contain insuffi cient descriptions from Heward Creek. Finally, many Terranes. Geological Society of America Memoir 159, thanks go to J. Allen, W. Gallin, J. Gooley, P. Dooling , p. 241–254, doi: 10 .1130 /MEM159 -p241 . feldspars and angular grains to have sourced the L. Pettinga, A. Turner, W. Benhallam, B. Chentnik, Beitler, B., Parry, W.T., and Chan, M.A., 2005, Fingerprints quartzofeldspathic fl uvial sandstones in the Kai- J. Mulhern, and R. Purcell for helpful discussions of fl uid fl ow: Chemical diagenetic history of the Juras- and contributions in the fi eld. We especially thank sic Navajo Sandstone, southern Utah, USA. Journal of parowits Basin. Additionally, units in the Sevier Sedimentary Research, v. 75, p. 547–561, doi:10 .2110 fold-and-thrust belt contain many age peaks N. Riggs, B. McConnell, P. DeCelles, and an anony- /jsr .2005 .045 . mous reviewer for valuable feedback and revisions. that are absent or insignifi cant in the Straight Bilodeau, W.L., 1986, The Mesozoic Mogollon Highlands, Arizona: An Early Cretaceous rift shoulder. The Jour- Cliffs Formation, and they rarely yield exclu- REFERENCES CITED nal of Geology, v. 94, p. 724–735, doi:10 .1086 /629077 . sively the 1.4 Ga and 1.7 Ga peaks present in Bilodeau, W.L., and Lindberg, F.A., 1983, Early Cretaceous Straight Cliffs fl uvial strata. 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