Stratigraphic Trends in Detrital Zircon Geochronology of Upper

Home , Miogeocline

Stratigraphic trends in detrital zircon geochronology of upper Neoproterozoic and Cambrian strata, Osgood Mountains, Nevada, and elsewhere in the Cordilleran miogeocline: Evidence for early Cambrian uplift of the Transcontinental Arch

Gwen M. Linde1, Patricia H. Cashman1, James H. Trexler, Jr.1, and William R. Dickinson2 1Department of Geological Sciences and Engineering, University of Nevada, Reno, Nevada 89557, USA 2Department of Geosciences, University of Arizona, Tucson, Arizona 85721-0077, USA

ABSTRACT a funda mental feature of the lower Paleozoic strata that reflect initial rifting (e.g., Poole Laurentian craton. It was ﬁ rst recognized from et al., 1992; Yonkee et al., 2014, and references U-Pb detrital zircon geochronology pro- broad structures and Phanerozoic sedimentation therein). These strata are mostly quartzite, with vides insight into the provenance of the patterns in the mid-continent (Fig. 1) (Keith, some siltstone, argillite, and phyllite; carbon- upper Neoproterozoic–lower Cambrian 1928). Sloss (1963, 1988) noted the deposition ate intervals are present in some locations (e.g., Osgood Mountain Quartzite and the upper of the middle and lowermost upper Cambrian Stewart, 1991; Poole et al., 1992). These units Cambrian–lower Ordovician Preble Forma- Sauk II sequence onlapping from the craton have been correlated across a broad region of tion in the Osgood Mountains of northern margin onto the Transcontinental Arch (Fig. 1). western North America (e.g., Poole et al., 1992). Nevada (USA). We analyzed 535 detrital zir- Carlson (1999) proposed, instead of a discrete Previous detrital zircon studies of upper Neo- con grains from six samples of quartz arenite arch, a platform, a discontinuous zone with proterozoic–lower Paleozoic passive margin by laser ablation–multicollector–inductively highs and lows and ﬂ anking basins that give the strata record similar changes in detrital zircon coupled plasma–mass spectrometry. The appearance of an arch (Fig. 1). age peaks and groups and therefore possibly detrital zircon age data of these Neo protero- In recent U-Pb detrital zircon geochronol- similar changes in provenance. Zircon ages in zoic–lower Paleozoic passive margin units ogy studies, researchers have proposed the upper Neoproterozoic–lower Cambrian strata in record a provenance change within the Transcontinental Arch as a barrier to sediment Utah (Lawton et al., 2010; Gehrels and Pecha, Osgood Mountain Quartzite. Comparison delivery from the central Laurentian craton to its 2014; Yonkee et al., 2014), Idaho (Yonkee et al., of these data with the work of others reveals western margin in early Paleozoic time (Amato 2014), and Nevada (Gehrels and Pecha, 2014; that this change in provenance occurred in and Mack, 2012; Gehrels and Pecha, 2014; Yonkee et al., 2014) change from predomi- correlative strata throughout an east-west Yonkee et al., 2014). Amato and Mack (2012) nantly Mesoproterozoic in the older strata to transect of the Great Basin. From latest Neo- documented evidence from the Bliss Sandstone upper Mesoproterozoic–Paleoproterozoic in the proterozoic through earliest Cambrian time, for the existence of the Transcontinental Arch younger strata. most grains were shed from the 1.0–1.2 Ga by at least the late Cambrian; they explained The only previous detrital zircon study of the Grenville orogen. After that time, drain- the differences in detrital zircon populations Osgood Mountain Quartzite was that of Gehrels age patterns changed and most grains were between the Tapeats Sandstone west of the arch and Dickinson (1995), who sampled from the derived from the 1.6–1.8 Ga Yavapai and and the Cambrian sandstones east of the arch by upper part of the formation. The Preble Forma- Mazatzal provinces; very few grains from the the uplift of the arch possibly as early as early tion has never been the subject of a published Grenville orogen were found in the younger Cambrian time. Gehrels and Pecha (2014) esti- detrital zircon study. strata. We suggest that this shift records the mated the uplift of the arch by early Cambrian We dated detrital zircons from three localities uplift, in early Cambrian time, of the Trans- time. Others have noted the possibility of early of the upper Neoproterozoic–lower Cambrian continental Arch. Our data also support our Cambrian uplift of the arch as the cause of the Osgood Mountain Quartzite and three locali- interpretation that the Osgood Mountain differences in detrital zircon age peaks and ties of the upper Cambrian–lower Ordovician Quartzite and the Preble Formation are cor- groups in passive margin strata in Utah (Yonkee Preble Formation in the Osgood Mountains relative to other contemporaneous passive et al., 2014). and near Edna Mountain, north-central Nevada margin strata in western Laurentia. Upper Neoproterozoic–lower Cambrian silici- (Fig. 2B; Table 1). We show that the detrital clastic rocks on the western Laurentian passive zircon ages shift within the Osgood Moun- INTRODUCTION margin record sedimentation that initiated after tain Quartzite; detrital zircons from the older rifting and continental separation (e.g., Stewart, samples are predominantly Mesoproterozoic, The Transcontinental Arch, a region of 1972; Poole et al., 1992). These passive mar- while detrital zircons from the younger sample, uplift that extends from the southwestern U.S. gin rocks were deposited on a discontinuously and all of the Preble Formation samples, are to south-central Ontario, Canada (Fig. 1), is exposed succession of diamictite and volcanic predominantly upper Mesoproterozoic–Paleo-

Geosphere; December 2014; v. 10; no. 6; p. 1402–1410; doi:10.1130/GES01048.1; 7 ﬁ gures; 1 table; 1 supplemental ﬁ le. Received 4 March 2014 ♦ Revision received 1 August 2014 ♦ Accepted 10 August 2014 ♦ Published online 7 October 2014

Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/10/6/1402/3338869/1402.pdf by guest on 28 September 2021 Detrital zircon geochronology of the Osgood Mountain Quartzite and Preble Formation in Nevada

50N passive margin section from the northwest U.S. 140W0 100W100W 60W to Sonora, Mexico (e.g., Lawton et al., 2010; SU CordilleranCordilleran HE Gehrels and Pecha, 2014; Yonkee et al., 2014). PassivePassive MMarginargin In contrast, the 1.8–1.6 Ga Yavapai-Mazatzal CanadaCanada Peri-LaurentianPeri-Laurentian and 1.48–1.34 Ga mid-continent granite rhyo- USA Peri-GondwananPeri-Gondwanan CORD WY lite provinces within the North America craton (720–400(720–400 MaMa)) (Fig. 1) were the dominant sediment sources Grenville orogen higher in the passive margin section (e.g., (1.2–1.0(1.2–1.0 Ga)Ga) ? ? Lawton et al., 2010; Gehrels and Pecha, 2014; 1.48–1.341.48–1.34 GaGa ? MMagmaticagmatic ProvProv ? NorthNorth Yonkee et al., 2014). The Osgood Mountain Quartzite and Preble Mazatzal/YavapaiMazatzal/Yavapai ? (1.8–1.6(1.8–1.6 Ga)Ga) ? Formation in northern Nevada have been inter- TTrans-Hudsonrans-Hudson ? APP 30N (2.0–1.8(2.0–1.8 GaGa)) USAU preted as passive margin strata; they both have ? ArcheanArchean ((>2.5>2.5 GaGa)) MexicoM co ? an interesting position and tectonic and meta- OA morphic histories. They are far to the west of Transcontinental Arches most other passive margin units and are over- Carlson (1999) thrusted by both the Roberts Mountains alloch- Sloss (1988) 1000 kmkm thon and the Golconda allochthon (Burchfi el Keith (1928) et al., 1992; Poole et al., 1992). The Preble Formation is metamorphosed to greenschist ? Mazatzal/Yavapai ? Boundary facies, and has refolded folds (Cashman et al., 2011); it has been interpreted as being in con- formable stratigraphic succession with the Figure 1. Location of the main age provinces in North America that are potential source Osgood Mountain Quartzite (Fig. 3), based on terranes for the late Neoproterozoic–early Cambrian western Laurentian passive margin. map relationships and compositional similarity Hypothesized transcontinental arches are superimposed (Keith, 1928; Sloss, 1988; Carlson, of an upper member of the Osgood Mountain 1999). WY—Wyoming province; HE—Hearn province; SU—Superior province; CORD— Quartzite to the Preble Formation (Hotz and Cordilleran; APP—Appalachian; OA—Ouachita-Marathon. Figure is after Gehrels et al. Willden, 1964). (2011) and adapted from Anderson and Morrison (1992), Bickford et al. (1986), Hoffman Structurally, the Osgood Mountains comprise (1989), Burchfi el et al. (1992), Bickford and Anderson (1993), Van Schmus et al. (1993), a large, northeast-trending anticline with a sub- Dickinson and Lawton (2001), and Dickinson and Gehrels (2009). horizontal axis (Fig. 2B). The Preble Formation is exposed only on the fl anks of the anticline proterozoic. Coeval passive margin strata in margin units? (4) If a consistent stratigraphic (Fig. 2B). Late Paleozoic rocks are thrust over other studies throughout the Great Basin (e.g., pattern of detrital zircon ages exists in all Neo- the anticline in the northern and western parts of Lawton et al., 2010; Gehrels and Pecha, 2014; proterozoic–Cambrian sections, what caused a the range, and the southern extent of the Osgood Yonkee et al., 2014) show the same shift in ages. widespread change in detrital zircon ages with Mountains is overlain by Cenozoic andesite This suggests that a change in provenance in time in these units? fl ows (Fig. 2B) (Hotz and Willden, 1964). The these passive margin strata is widely recorded in Osgood Mountain Quartzite and Preble Forma- this region of western Laurentia. GEOLOGIC SETTING tion are primarily exposed in the central and In this paper we present new U-Pb zircon southern portions of the range (Fig. 2B). ages from the Osgood Mountain Quartzite and The North American craton contains several The Osgood Mountain Quartzite consists the Preble Formation. The dates were obtained Proterozoic and Archean age provinces, thus mostly of fi ne- to medium-grained quartz using laser ablation–multicollector–inductively providing geographically distinguishable crustal arenite, with some silty and shaly beds (Fig. 3). coupled plasma–mass spectrometry (LA-MC- provinces that are source terranes for the upper The formation crops out in the Osgood Moun- ICP-MS). We compare these new data with the Proterozoic and lower Paleozoic continental tains in a belt 14 km long, from the northwest- detrital zircon ages of coeval passive margin margin sedimentary section (e.g., Gehrels et al., ern Osgood Mountains near Goughs Canyon, strata throughout the Great Basin to evaluate 2011, and references cited therein) (Fig. 1). The to the Golconda Mine area in the northwest- provenance and sediment transport patterns, and Yavapai-Mazatzal province (1.8–1.6 Ga) forms ern part of Edna Mountain (Fig. 2B). Goughs the possibility that these patterns were altered the core of the craton in the U.S. (Fig. 1). It is Canyon and the Golconda Mine, where two by the uplift of the Transcontinental Arch. bound on the northwest by the Trans-Hudson samples were taken, are on opposite fl anks of Several unsolved problems are addressed in orogenic terrane (2.0–1.8 Ga) and Archean an anticline and are relatively high in the strati- this study. (1) What is the provenance of the rocks (older than 2.5 Ga) of the Wyoming and graphic section (Figs. 2B and 3). Soldier Pass, Osgood Mountain Quartzite and the Preble For- Superior provinces (Fig. 1). It is bound on the where a third sample was collected, is closer mation? (2) Are the Osgood Mountain Quartzite east and southeast by the terranes of the Gren- to the core of the anticline and is thus lower in and Preble Formation passive margin units, as ville orogen (1.2–1.0 Ga) (Fig. 1). the stratigraphic section (Figs. 2B and 3). The others have interpreted? (3) Within the Osgood The 1.2–1.0 Ga Grenville orogen of south- base of the Osgood Mountain Quartzite is not Mountain Quartzite, there is a signifi cant ern and eastern North America (Fig. 1) was the exposed; the thickness has been estimated as change in detrital zircon grain ages. Are there dominant sediment source for western Laurentia >1524 m (Hotz and Willden, 1964). The upper similar patterns of detrital zircon grain ages throughout the Neoproterozoic (Rainbird et al., part of the Osgood Mountain Quartzite is the varying with time among other coeval passive 1997, 2012), including the upper Proterozoic Twin Canyon Member, which crops out only

Geosphere, December 2014 1403

Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/10/6/1402/3338869/1402.pdf by guest on 28 September 2021 Linde et al.

120°0ʹ0″W 110°0ʹ0″W 100°0ʹ0″W

A 50°0ʹ0″N

45°0ʹ0″N Idaho

Portneuf Osgood Range Mountains Pilot Huntsville Range (B) B Deep Creek Salt Lake 40°0ʹ0″N Range City Detrital Zircon Sample Locaon Snake Reno Range Canyon rch Cenozoic Andesites Range Nevada Cambrian - Ordovician Preble Formaon Utah Neoproterozoic - Cambrian Osgood California Las Vegas Grand New Mexico Mountains Quartzite Canyon

Transcontinental A 35°0ʹ0″N 117°28ʹW 117°24ʹW

Arizona 0 1500 3000 Southwest Meters New Mexico Goughs Canyon N Osgood 30°0ʹ0″N Mountains Hogshead Canyon

41°5ʹN

Soldier Pass Garden Spring

Figure 2. (A) Locations of study areas in the vicinity of the Osgood Mountains and in the Great Basin region (Transcontinental Arch is after Sloss, 1988). (B) Geologic map of the Osgood Mountains. The six sample locations are shown. Broad northeast-trending anticline of the range is shown with location of Soldier Pass sample in the core of the anticline and Preble Formation on both ﬂ anks of the anticline. Hogshead Canyon, the location of the unit 41°0ʹN thickness estimate of the Preble Formation, is shown. Northern part of the map is after Hotz and Willden (1964); southern part is after Erickson and Marsh (1974). Humboldt River

Golconda Mine

on the east side of the range, and consists of Formation, the Osgood Mountain Quartzite is et al. (1952) estimated the thickness of the Preble more silty and shaly material than the rest of the late Neoproterozoic to early Cambrian in age Formation as ~2350 m based upon the estimated formation. This member has been interpreted (Madden-McGuire, 1991). thicknesses of the subunits, although they sug- as a transition between the Osgood Mountain The Preble Formation consists of phyllite and gested that the structural thickness may exceed Quartzite and the overlying Preble Formation shale, interbedded limestone, and quartz arenite ; 4572 m due to isoclinal folding. The thickness (Hotz and Willden, 1964). The Osgood Moun- it crops out over an area ~50 km in length, from was estimated by Hotz and Willden (1964) as tain Quartzite has no fossils (Hotz and Willden, northwestern Osgood Mountain near Goughs ~1524 m near Hogshead Canyon (Fig. 2B), 1964). Based on the age of the overlying Preble Canyon south to the Sonoma Range. Ferguson where both upper and lower contacts are faults;

1404 Geosphere, December 2014

TABLE 1. LOCATIONS AND NUMBERS OF SAMPLES reverse discordance (105% concordance). Nor- REFERENCED TO UTM LOCATIONS malized probability plots (Fig. 5) allow visual Sample Easting Northing comparison between zircon populations and Cambrian–Ordovician Preble Formation Golconda Mine GOL-02-CP 0465271 4533874 display the data from this study and the research Garden Spring GS-01-CP 0470302 4548660 of others. The normalized probability plots are Goughs Canyon GC-01-CP 0468513 4554509 generated by summing the ages and uncertain- Neoproterozoic–Cambrian Osgood Mountain Quartzite ties and normalizing the graphs so that all curves Golconda Mine GOL-01-COM 0462354 4531791 on the same plot have the same area under Goughs Canyon GC-03-COM 0468951 4554410 Soldier Pass SP-01-COM 0463750 4548029 the curve. Note: NAD 83 UTM 11N (Universal Transverse Mercator North American We compared detrital zircon age distribu- Datum 1983). tions both visually and statistically. Our initial appraisal was visual comparison of the probability plots. We also compared many age distri- however, they noted that tight folding and lack of three samples were analyzed from the lower butions using the Kolmogorov-Smirnov (K-S) distinctive bedding precluded them from making Cambrian–lower Ordovician Preble Formation. statistic (Guynn and Gehrels, 2006). The K-S detailed studies of the thickness and stratigraphy Zircon grains were separated and analyzed at statistic estimates the probability (P value) of the unit. Based on middle-early Cambrian the University of Arizona LaserChron facility that two sample populations could have been trilobite fauna collected in the lower part of the using standard techniques described by Gehrels derived from the same parent population. P > Preble Formation, the base of the unit is early (2000, 2012), Gehrels et al. (2006, 2008), and 0.05 indicates >95% probability that two U-Pb Cambrian in age (Madden-McGuire, 1991). The Johnston et al. (2009), to yield a best age dis- distributions are not statistically different and fossils occur ~400 m above the upper contact tribution refl ective of the true distribution of could have been derived from the same parent of the pure quartz arenite Osgood Mountain detrital zircon ages in each sample. A split of (P = 1.0 refl ects effective statistical identity). Quartzite, consistent with a late Neoproterozoic zircons representative of the fi nal sample yield The K-S statistic is sensitive to proportions of age for most of the Osgood Mountain Quartzite was mounted in a 2.54-cm-diameter epoxy ages present, and a low P value may indicate (Madden-McGuire, 1991). Graptolites near the plug, with the laboratory’s SL (Sri Lanka) zir- that the proportions of ages are different, even youngest subunit of the Preble Formation indi- con standard (563.5 ± 3.2 Ma; Gehrels et al., though the ages are similar (Gehrels, 2012). cate that the top of the unit is Early Ordovician 2008). Approximately 100 randomly selected (Madden-McGuire, 1991). grains were analyzed for each sample. Analyses DETRITAL ZIRCON were conducted by LA-MC-ICP-MS using the GEOCHRONOLOGY RESULTS METHODS New Wave UP193HE laser connected to the Nu Plasma high-resolution ICP-MS. Osgood Mountain Quartzite (Upper Quartz arenite samples were collected from Analytical results are displayed graphically Neoproterozoic–Lower Cambrian) six locations and stratigraphic intervals (Figs. on normalized probability plots (Figs. 4 and 2B and 3; Table 1). Three samples were ana- 5). We did not include analyses with >10% Two samples from near the top of the Osgood lyzed from the upper Neoproterozoic–lower uncertainty in age, and discarded analyses with Mountain Quartzite, collected at Goughs Can- Cambrian Osgood Mountain Quartzite and >30% discordance (70% concordance) and >5% yon and Golconda Mine (Figs. 2B and 3; Table 1), and one sample from ~400 m below the top of the unit, collected at Soldier Pass (Figs. 2B and 3; Table 1), were analyzed. U-Pb Pennsylvanian Iron Point Conglomerate data and location information for each sample Ordovician analyzed in this study is provided in the Sup- plemental Table1. Our visual and statistical Detrital Zircon Sample ? analyses indicate that the Mesoproterozoic and Preble Formation Paleoproterozoic detrital zircon age groups of the two younger samples are similar, although

Cambrian GOL-02-CP the proportions of ages are somewhat differ- GS-01-CP ent (see Appendix 1 for a discussion of statis- GC-01-CP

approx. 4000 m tical analysis). The detrital zircon age groups GC-03-COM from these two samples are quite different; the GOL-01-COM older sample is dominated by Mesoproterozoic Osgood Mountain grains, while the younger sample is dominated ? Quartzite SP-01-COM by Paleoproterozoic grains (Fig. 4). K-S test Neoproterozoic (base not exposed) results conﬁ rm that these detrital zircon grain populations are dissimilar: P is <0.05. Figure 3. Stratigraphic column of the Osgood Mountain Quartzite and Preble Formation. Subjacent strata are not shown. Red dashed 1Supplemental Table. U-Pb data for each sample lines are approximate system boundaries. The Iron Point normal analyzed in this study, including location informa- fault shown is mid-Pennsylvanian. Structural relationships are after tion. If you are viewing the PDF of this paper or reading it ofﬂ ine, please visit http:// dx .doi .org /10 Cashman et al. (2011); unit ages are after Hotz and Willden (1964) .1130/GES01048 .S1 or the full-text article on www and Madden-McGuire (1991). .gsapubs .org to view the Supplemental Table.

Geosphere, December 2014 1405

Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/10/6/1402/3338869/1402.pdf by guest on 28 September 2021 Linde et al.

Figure 4. Normalized probability plots of 1704 units sampled in and around the Osgood 1429 Mountains. The curves contain all analy- Preble Formation ses for each unit and are normalized such Golconda Mine that the area is the same under each curve. (GOL-02-CP) Within each location the older units are on (n=95) the bottom. Horizontal axis is age in millions 1702 of years. Number of concordant detrital zir- 1440 Preble Formation cons in each sample is shown in parentheses. Garden Spring (n=88) (GS-01-CP)

1694 1428 Preble Formation (Lower Cambrian– Preble Formation Lower Ordovician) Goughs Canyon (GC-02-CP) The three Preble Formation samples were (n=90) collected low in the formation (Fig. 3) at 1783 Goughs Canyon, Garden Spring, and Golconda Mine (Fig. 2B; Table 1). The samples all con- tained Paleoproterozoic and Mesoproterozoic age peaks (Fig. 4). Applying the K-S test, we 1423 Osgood Mountain Quartzite found that within the Preble Formation, the Goughs Canyon

three different sample pairs have P values of Probability Age (GC-03-COM) 0.849, 0.881, and 0.937. All sample pairs of the Preble Formation and Osgood Mountain (n=87) Quartzite have P values <0.05. 1782

DISCUSSION Osgood Mountain Quartzite 1422 Golconda Mine Osgood Mountain Quartzite (GOL-01-COM) (n=89) The source of the detrital zircon grains in the 1053 Osgood Mountain Quartzite samples is Lauren- tian, and the samples have two distinct prove- nances. The change in detrital zircon ages from the older Soldier Pass sample to the younger Osgood Mountain Quartzite Goughs Canyon and Golconda Mine samples 1701 Soldier Pass indicates a signiﬁ cant change in provenance (SP-01-COM) during the deposition of the Osgood Mountain (n=86) Quartzite. The grains from Soldier Pass are pre- 0 500 1000 1500 2000 2500 3000 3500 4000 dominantly Mesoproterozoic (Fig. 4) and we interpret that their source was the 1.2–1.0 Ga Detrital Zircon Age (Ma) Grenville orogen (Fig. 1). There are also some Paleoproterozoic grains which we interpret to have been derived from the 1.8–1.7 Ga Yavapai Archean province and the 2.0–1.8 Ga Trans-Hudson Neoproterozoic orogen (Fig. 1). There are a few Mesoprotero- Mesoproterozoic Paleoproterozoic zoic grains; these are interpreted to have been shed from the 1.48–1.34 Ga mid-continent provinces (Fig. 1). Archean grains are inter- Mesoproterozoic grains predominate in all three granite-rhyolite provinces (Fig. 1). In contrast, preted to have been sourced from the Archean samples (Fig. 4) and are interpreted to have been the detrital zircon ages in the Goughs Canyon craton (Fig. 1). A few Mesoproterozoic grains shed from the 1.48–1.34 mid-continent granite- and Golconda Mine samples (Fig. 4) share age are interpreted to have been derived from the rhyolite provinces (Fig. 1). A large number of peaks, and these peaks are different from those 1.2–1.0 Ga Grenville orogen (Fig. 1). Paleoproterozoic grains are interpreted to have of the Solider Pass sample (Fig. 5). The Paleo- been derived from the 1.7–1.62 Ga Mazatzal proterozoic grains in these samples are inter- Preble Formation province and the 1.8–1.7 Ga Yavapai province preted to have been shed from the 1.8–1.7 Ga (Fig 1). A smaller number of Mesoproterozoic Yavapai province and the 1.7–1.62 Ga Mazat- The detrital zircon ages in all three Preble grains are interpreted as having their source in zal province (Fig. 1). Mesoproterozoic grains Formation samples are similar (Fig. 4). We the 1.2–1.0 Ga Grenville orogen (Fig. 1). The are interpreted to have been shed from the interpret that these three Preble Formation remaining grains are Archean and their source is 1.48–1.34 Ga mid-continent granite-rhyolite samples share a common Laurentian source. interpreted as the Archean craton (Fig. 1).

1406 Geosphere, December 2014

Creek Group (Fig. 6). In all three ranges, the McCoy Creek Group has similar Mesoprotero-

(n=94) Upper Windyndy PassPPasass AArgillite zoic age groups and peaks (Fig. 5) (Yonkee Portneuf et al., 2014). We interpret these grains as pri- Range (n=38) Middle Windyndydy Pass AArArgillite Idaho marily shed from the 1.2–1.0 Ga Grenville (n=58) Middle Caddy Canyonanyon QuartziteQuQ a orogen and the 1.48–1.34 Ga mid-continent granite-rhyolite province (Fig. 1). This is simi- Geersten Canyonanyon QuQuartzitea lar to the older Osgood Mountain Quartzite (n=179) Huntsville (Soldier Pass) sample, which we interpreted to Brown’ss Hole ForFoFormationm (n=94) Utah be sourced in these same terranes. The younger (n=66) MutualMutual FoFormationForm strata in all three ranges are the Cambrian Pros- pect Mountain Quartzite, and in the Deep Creek (n=83) Kelley Canyonaanyonnyon ForFormationF m Range, the Cambrian Busby Formation (Fig. 6). In all three ranges, the detrital zircons in these (n=99) Prospect Mountainoountainuntain QuartziteQu Pilot Range younger strata have similar Paleo proterozoic (n=56) McCoyCCoyoy Creek Group Nevada and Mesoproterozoic age groups and peaks (n=83) McCoyCCoyoy Creek Group (Fig. 5) (Yonkee et al., 2014). We interpret these grains as shed from the 1.80–1.70 Ga BusbyBusby FFormationFororm (n=79) Deep Creek Yavapai province and the 1.34–1.48 Ga mid- (n=93) Prospect Mountainoountainuntain QuartziteQu Range continent granite-rhyolite province (Fig. 1), (n=83) McCoyCCoyoy Creek Group Utah very similar to the younger Osgood Mountain Quartzite samples. (n=95) Prospect Mountainoountainuntain QuartziteQu Snake Range (n=95) McCoyCoy Creek Group Nevada Central Utah: Canyon Range (n=89) Prospect Mountainoountainuntain QuartziteQu Canyon (n=86) Caddy CanyonCanyon QuQuartziteQu Range Detrital zircons in Canyon Range strata Utah PPreblereble FoFFormationorm (Fig. 2A) indicate a shift of ages similar to (this(this study) (n=273) those analyzed in the Osgood Mountains. The Osgood Mountainountainuntain QuQuartzitea older unit analyzed in the Canyon Range is (Gehrelss & PechaPech 2014) (n=209) Osgood the Neo protero zoic Caddy Canyon Quartz- Mountains Osgood Mountainoountainuntain QuQQuartziteu ite (Fig. 4). This unit has Mesoproterozoic (this study; GoughsGough CCanyon Nevada andd GolcondaGolcondGolco a Mine) age groups and peaks (Fig. 5) (Lawton et al., (n=176) 2010) that we interpret as primarily from the Osgood Mountainoountainuntain QuQQuartziteu (n=86) (this study;ddy;y; SoldierSoldier Pass) 1.2–1.0 Ga Grenville orogen and the 1.48– 1.34 Ga mid-continent granite-rhyolite province (Fig. 1). These age peaks and our source area interpretation are very similar to those of the older Osgood Mountain Quartzite sample. Archean Craton Grenville Orogen Mazatzal Yavapai Trans-Hudson Orogen Granite Rhyolite The younger unit in the Canyon Range is Detrital Zircon Age (Ma) the Cambrian Prospect Mountain Quartzite (Fig. 6). This unit has Paleoproterozoic and Figure 5. Plots of detrital zircon age of each Neoproterozoic–Cambrian unit organized Meso protero zoic age groups and peaks (Fig. 5) by locality (see map in Fig. 1) showing the distribution of detrital zircon ages. Curves (Lawton et al., 2010). We interpret these detrital are normalized probability plots. The number of detrital zircon grains composing each zircons as shed from the 1.80–1.70 Ga Yavapai analysis is shown on the left. Within each location the older units are on the bottom. province and the 1.48–1.34 Ga mid-continent The vertical shaded bars show principal ages of zircons that would have been shed from granite-rhyolite province (Fig. 1), similar to the potential source regions; colors are the same as those in Figure 1. Canyon Range— younger Osgood Mountain Quartzite samples. Lawton et al. (2010); Snake, Deep Creek, and Pilot Ranges, Huntsville, and Portneuf Range—Yonkee et al. (2014); Osgood Mountains—Linde et al. (2012); Gehrels and Northeastern Utah: Huntsville Pecha (2014). Detrital zircons from Huntsville samples (Fig. 2A) record a shift of ages comparable REGIONAL CORRELATION Nevada-Utah Border: Deep Creek, to those analyzed in the Osgood Mountains. Pilot, and Snake Ranges The older units in the Huntsville section Detrital zircon ages in passive margin strata are the Neoproterozoic Kelley Canyon and across a transect of the Great Basin vary strati- Detrital zircons from rocks in the Deep Mutual Formations and the Neoproterozoic– graphically in a manner similar to those we Creek, Pilot, and Snake Ranges (Fig. 2A) Cambrian Brown’s Hole Formation (Fig. 6). documented within the Osgood Mountain record a shift of ages similar to that of detrital The Kelley Canyon Formation (Yonkee et al., Quartzite, recording a major regional change in zircons analyzed in the Osgood Mountains. The 2014), the Mutual Formation (Stewart et al., provenance. older strata are of the Neoproterozoic McCoy 2001; Yonkee et al., 2014), and the Brown’s

Geosphere, December 2014 1407

Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/10/6/1402/3338869/1402.pdf by guest on 28 September 2021 Linde et al.

Osgood Mountains Snake & Pilot Deep Creek Ca n y on R a nge Hunts vill e Por tn euf Range Grand Canyon Southwest Nevada Range Nevada Range Utah Utah Utah Idaho Arizona New Mexico (this study) (Yonkee et al., (Yonkee et al., (Lawton et al., (Yonkee et al., (Yonkee et al., (Gehrels et al., (Amato & 2014) 2014) 2010) 2014) 2014) 2011) Mack, 2012) Bliss Preble SS Busby Fm Prospect Geersten Cambrian Fm Prospect Cyn Qtz Windy Pass Tapeats Sauk Mtn Qtz Prospect Mtn Qtz Argillite SS 540 Ma Mtn Qtz Brown’s Sequence Osgood Mutual Neo- McCoy McCoy Hole Fm } Mtn Qtz Creek Gp Fm Mutual proterozoic Creek Gp Mutual Caddy Fm Fm Caddy Cyn Qtz Cyn Qtz Kelley Caddy Detrital Zircon sample Kelley Cyn Qtz Cyn Fm Cyn Fm

Figure 6. Stratigraphic columns of the passive margin strata discussed in text. Subjacent strata are not shown. Neoproterozoic-Cambrian boundary at 540 Ma is approximated for each location. Strata in the Osgood Mountains are shown in stratigraphic succession and are correlative with regional passive margin strata. Only the detrital zircon samples referenced in the text are shown. Abbreviations: Mtn—mountains; Qtz—quartzite; Fm—formation; Gp—group; Cyn—canyon; SS—sandstone.

Hole Formation (Yonkee et al., 2014) have Implications of the Regional Correlation Grenville orogen and the detrital zircons of the similar Mesoproterozoic age groups and peaks younger strata are predominantly the age of (Fig. 5). We interpret these grains as primarily In the ﬁ ve areas of the passive margin exam- the Yavapai province basement rocks. derived from the 1.2–1.0 Ga Grenville orogen ined, the detrital zircon age patterns change in a The shift in detrital zircon age across the and the 1.48–1.34 Ga mid-continent granite- systematic way (Fig. 7). The detrital zircons of region implies a provenance change across the rhyolite province (Fig. 1), very similar to our the older strata are predominantly the age of the region at approximately the same time. Conti- older Osgood Mountain Quartzite sample. The younger unit in the Huntsville section is the Cambrian Geersten Canyon quartzite (Fig. 6). North- PreblePreble FoFormationrrm Central The Geersten Canyon quartzite (Stewart (n=273) Nevada et al., 2001; Yonkee et al., 2014) has Meso- Windyndy PassPass AArgillite Geersten CanyonCCananyon QuartziteQuQu proterozoic, Paleoproterozoic, and Archean Brown’ss HoleHole FormFormationFor Utah/Idaho/ BBusbyusby FFormFormationor age groups and peaks (Fig. 5). We interpret Prospect Mountainoountainuntain QuQuartziteQ E Nevada these grains as derived primarily from the (n=881)Younger 1.80–1.70 Ga Yavapai province and second- Strata Osgood Mountainountainuntain QuQuaQuartzitea North- arily from the 1.2–1.0 Ga Grenville orogen (GoughsGGoughsoughs CCaCanyon and Golconda Mine) Central and the 2.5 Ga and older Archean craton (n=176) Nevada (Fig. 1). These age peaks and our interpreted provenance are similar to that for our younger Middle Caddy CanyonCanyon QuQuartziteQu Osgood Mountain Quartzite samples. MMutualutual FFormFormationor Utah/Idaho/ Kelley Canyonaannyon FoFormationFormr McCoyCCoyoy Creek Group E Nevada Caddy CanyonCanyon QuartziteQuQu Southeastern Idaho: Portneuf Range (n=650)

Detrital zircons from rocks in the Portneuf Older North- Range (Fig. 2A) record a shift of ages similar Osgood Mountainoountainuntain QuQQuartziteu Central Strata ((SoldierSoldier Pass) to those analyzed in the Osgood Mountains. In (n=86) Nevada the Portneuf Range, the older unit is the Neo- proterozoic Middle Caddy Canyon Quartzite (Fig. 6). The Middle Caddy Canyon Quartz- ite has Mesoproterozoic age groups and peaks Archean Craton Grenville Orogen Mazatzal Yavapai Trans-Hudson Orogen (Fig. 5) (Yonkee et al., 2014). We interpret these Granite Rhyolite grains as primarily shed from the 1.2–1.0 Ga Detrital Zircon Age (Ma) Grenville orogen (Fig. 1). These age peaks and our source area interpretation are very similar Figure 7. Plots of compilations of units showing the distribution of detrital zircon ages. to that of the older Osgood Mountain Quartzite Curves on the upper part of the ﬁ gure are compilations of the younger strata throughout the sample. The younger unit in the Portneuf Range region, compared with the younger strata in our pilot study. Curves on the lower part of the is the Windy Pass Argillite, comprising upper ﬁ gure are compilations of the older strata throughout the region, compared with the older and middle members (Fig. 6); both members strata in our pilot study. Curves are normalized probability plots. The number of detrital have Paleoproterozoic age peaks and groups zircon grains composing each analysis is shown on the left. The thinner lines are from our (Fig. 5) (Yonkee et al., 2014). We interpret these pilot study; the thicker lines are the composites of data from elsewhere in the Basin and grains as shed from the 1.80–1.70 Ga Yavapai Range. Canyon Range—Lawton et al. (2010); Snake, Deep Creek, and Pilot Ranges, Hunts- province (Fig. 1). This is very similar to the ville, and Portneuf Range—Yonkee et al. (2014); Osgood Mountains—Linde et al. (2012); younger Osgood Mountain Quartzite sample. Gehrels and Pecha (2012).

1408 Geosphere, December 2014

nent-spanning river systems carried sands from North American craton, and that the sources Scott Johnston for sharing their data and providing the Grenville orogenic terrane across the Lau- changed with time. The oldest sample of the valuable input. Analyses reported herein were conducted at the Arizona LaserChron Center, which is rentian continent to the western passive margin Osgood Mountain Quartzite, taken near Soldier supported by NSF grants EAR-0732436 and EAR- in late Neoproterozoic to early Cambrian time Pass, was derived primarily from the Grenville 1032156. We also thank the following for supporting (e.g., Rainbird et al., 1997; Cawood and Nem- orogen. The younger Osgood Mountain Quartz- Linde’s graduate studies: the NSF Graduate Research chin, 2001; Mueller et al., 2007; Dehler et al., ite samples were derived primarily from the fellowship program, the Rocky Mountain Association 2010; Kingsbury-Stewart et al., 2013). By Yavapai and Mazatzal provinces. The strati- of Geologists Veterans Memorial Scholarship, the Nevada Petroleum and Geothermal Society, Raytheon early to middle Cambrian time (as found in this graphically overlying Preble Formation was Corporation’s Student Veterans Scholarship, and the study), river systems were carrying relatively also derived primarily from the Yavapai and U.S. Veterans Administration Post-9/11 GI Bill. We very few Grenville-aged detrital zircons to the Mazatzal provinces. thank Daniel Sturmer, Ross Miller, and Connor New- passive margin in the areas that we investigated. The shift in age peaks and groups of detrital man for their assistance with fi eld work and laboratory analyses. Our data support the proposal that the Trans- zircons within the Osgood Mountain Quartzite continental Arch, a continent-scale crustal section is also recorded in other passive margin APPENDIX 1. STATISTICAL feature that was not present in the middle strata in Nevada, Utah, and Idaho. This shift ANALYSIS OF OSGOOD MOUNTAIN Neoproterozoic, was uplifted in the latest Neo- indicates a widespread change in provenance; QUARTZITE SAMPLES proterozoic or earliest Cambrian. The uplifted the older passive margin units were derived arch provided vertical relief, and forced a primarily from the Grenville orogen and the A visual scan of the Goughs Canyon and Golconda change in sedimentation and drainage patterns, younger units were derived primarily from the Mine relative probability graphs (Figs. 6 and 7) reveals similar age peaks, with similar numbers of grains, ca. restricting the transport of sediment from the more proximal Yavapai and Mazatzal provinces. 1700 Ma. Both of these graphs also show peaks ca. Grenville orogenic terrane to western Laurentia. Our data support the proposal that the wide- 2500 Ma and 2900 Ma, although different numbers of This gradual change in drainage patterns caused spread and time-correlative shift in provenance grains form the peaks. The K-S statistical test found the observed dearth of Grenville-age zircons. of passive margin strata across the Great Basin very low correlation (P < 0.05) between these two samples when we compared the entire data set for The uplift of the arch also would have exposed records the uplift of the Transcontinental Arch. each sample. However, the K-S test is very sensitive basement rocks of the Archean craton, the In late Neoproterozoic time, these passive mar- to proportions of ages, and as with these samples, will Trans-Hudson orogen, the Yavapai and Mazat- gin units were sourced primarily in the Gren- indicate no or low correlation, although a visual exam- zal terranes, and the mid-continent anorogenic ville orogen; by the early Cambrian, most pas- ination coupled with geologic understanding indicates granites (Fig. 1). Sloss (1963) demonstrated that sive margin units were sourced primarily from the contrary, i.e., a high likelihood of common sources (Gehrels, 2012). Within the Osgood Mountain Quartz- the Sauk sequence onlapped basement rocks the Yavapai and Mazatzal provinces with very ite, we used the K-S statistical test to compare the by middle Cambrian time; this onlap requires little input from the Grenville orogen. The pre- distinct Neoproterozoic and Archean grain subpopu- that the basement rocks were exposed. These dominantly east to west paleocurrents (Seeland, lations. The correlation between the Goughs Canyon uplifted and exposed basement rocks became 1968) carried Grenville sands from the eastern and Golconda Mine Neoproterozoic subpopulations was 0.957, while the correlation between the Archean the sources for the sediments draining from third of the craton to the western passive mar- subpopulations of these two samples was 0.174. This the western fl ank of the Transcontinental Arch gin until early Cambrian time, when the Trans- comparison of subpopulations allows us to account to the western Laurentian margin. The uplift of continental Arch was uplifted and blocked this the different proportions of grains of similar ages that the arch caused the preponderance of zircons sediment dispersal pattern, and provided a new would otherwise indicate no correlation. of the age of the Trans-Hudson orogen and the sediment source for western Laurentia. Our REFERENCES CITED Yavapai, Mazatzal, and mid-continent granite results corroborate previous suggestions that the provinces in the younger passive margin strata Transcontinental Arch blocked the transport of Amato, J.M., and Mack, G.H., 2012, Detrital zircon geo- investigated in this study. sediments in the early Paleozoic (Amato and chronology from the Cambrian–Ordovician Bliss Sand- stone, New Mexico: Evidence for contrasting Gren- Across the Great Basin transect investigated Mack, 2012; Gehrels and Pecha, 2014; Yonkee ville-age and Cambrian sources on opposite sides of the for this study, the defi nitive shift in detrital zir- et al., 2014). This study substantiates the pre- Transcontinental Arch: Geological Society of America con age spectra records a tectonic event that vious interpretations by demonstrating coeval Bulletin, v. 124, p. 1826–1840, doi: 10 .1130 /B30657 .1 . Anderson, J.L., and Morrison, J., 1992, The role of anoro- caused a coeval change in sediment transport shifts in provenance across a broad transect of genic granites in the Proterozoic crustal development patterns. This detrital zircon age shift therefore the Great Basin and confi rms that the uplift of of North America, in Condie, K.C., ed., Proterozoic could be a useful correlation tool. Such a tool the arch was suffi cient to change drainage pat- Crustal Evolution: New York, Elsevier, p. 263–299. Bickford, M.E., and Anderson, J.L., 1993, Middle Protero- would be particularly helpful in dating quartz terns by early Cambrian time. zoic magmatism, in Reed, J.C., et al., eds., Precam- arenites, which are often lacking in biostrati- We propose that analysis and comparison brian: Conterminous U.S.: Boulder, Colorado, Geolog- ical Society of America, Geology of North America, graphic markers and thus diffi cult to date with of detrital zircon age signatures can be used to v. C-2, p. 281–292. confi dence. We suggest that stratigraphic sec- support other chronostratigraphic correlation Bickford, M.E., Van Schmus, R., and Zietz, I., 1986, tions documented by our work and others can tools, especially in fossil-poor and diffi cult to Protero zoic history of the midcontinent region of North America: Geology, v. 14, p. 492–496, doi:10 .1130 be correlated based on this consistent change in date quartz arenites. When used in conjunction /0091-7613 (1986)14 <492: PHOTMR>2 .0 .CO;2 . detrital zircon age peaks, and that other sections with other correlation methods, shifts in detrital Burchfi el, B.C., Cowan, D.S., and Davis, G.A., 1992, in the region can also be correlated in this way. zircon age spectra can provide important infor- Tectonic overview of the Cordilleran orogeny in the western United States, in Burchfi el, B.C., et al., eds., mation where other stratigraphic techniques are The Cordilleran Orogen: Conterminous U.S.: Boulder, SUMMARY AND CONCLUSIONS unavailable. Colorado, Geological Society of America, Geology of North America, v. G-3, p. 407–480. ACKNOWLEDGMENTS Carlson, M.P., 1999, Transcontinental Arch—A pattern U-Pb analyses of detrital zircons from the formed by rejuvenation of local features across central Osgood Mountain Quartzite and the Preble North America: Tectonophysics, v. 305, p. 225–233, Detrital zircon analyses were funded by National doi: 10 .1016 /S0040 -1951 (99)00005 -0 . Formation in northern Nevada demonstrate that Science Foundation (NSF) grant EAR-0510915 to Cashman, P.H., Villa, D.E., Taylor, W.J., Davydov, V.I., and these units were shed from sources within the Pat Cashman. We thank Paul Link, Tim Lawton, and Trexler, J.H., Jr., 2011, Paleozoic contractional and

Geosphere, December 2014 1409

Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/10/6/1402/3338869/1402.pdf by guest on 28 September 2021 Linde et al.

extensional deformation at Edna Mountain, Nevada: Gehrels, G.E., Valencia, V.A., and Ruiz, J., 2008, Enhanced logical Society of America, Geology of North Amer- Geological Society of America Bulletin, v. 123, precision, accuracy, effi ciency, and spatial resolution ica, v. G-3, scale 1:6,900,000. p. 651–668, doi: 10 .1130 /B30247 .1 . of U-Pb ages by laser ablation–multicollector–induc- Rainbird, R.H., McNicoll, J., Theriault, R.J., Heaman, L.M., Cawood, P.A., and Nemchin, A.A., 2001, Paleogeographic tively coupled plasma–mass spectrometry: Geo- Abbott, J.G., Long, D.G.F., and Thorkelson, D.J., development of the east Laurentian margin: Con- chemistry Geophysics Geosystems, v. 9, doi: 10 .1029 1997, Pan-continental river system draining Grenville straints from U-Pb dating of detrital zircons in the /2007GC001805 . orogeny recorded by U-Pb and Sm-Nd geochronology Newfoundland Appalachians: Geological Society of Gehrels, G.E., Blakey, R., Karlstrom, K.E., Timmons, J.M., of Neoproterozoic quartzarenites and mudrocks, north- America Bulletin, v. 113, p. 1234–1246, doi:10 .1130 Dickinson, B., and Pecha, M., 2011, Detrital zircon western Canada: Journal of Geology, v. 105, p. 1–17, /0016 -7606 (2001)113<1234: PDOTEL>2.0 .CO;2. U-Pb geochronology of Paleozoic strata in the Grand doi: 10 .1086 /606144 . Dehler, C.M., Fanning, C.M., Link, P.K., Kingsbury, E.M., Canyon, Arizona: Lithosphere, v. 3, p. 183–200, doi: Rainbird, R.H., Cawood, P., and Gehrels, G., 2012, The and Rybcynski, D., 2010, Maximum depositional age 10 .1130 /L121 .1 . great Grenvillian sedimentation episode: Record of and provenance of the Uinta Mountain Group and Big Guynn, J., and Gehrels, G.E., 2006, Comparison of detrital supercontinent Rodinia’s assembly, in Busby, C., and Cottonwood Formation, northern Utah: Paleogeog- zircon age distribution using the K-S test: University Azor, A., eds., Tectonics of Sedimentary Basins: Recent raphy of rifting western Laurentia: Geological Society of Arizona LaserChron Center online manual, 16 p., Advances: Hoboken, New Jersey, Blackwell Publish- of America Bulletin, v. 122, p. 1686–1699, doi:10 .1130 https:// docs .google .com /fi le /d/0B9ezu34P5h8eZWZm ing, p. 583–601, doi: 10 .1002 /9781444347166 .ch29 . /B30094.1 . OWUzOTItZDgyZi00NDRiLWI4ZTctNTljNTM5OT Seeland, D.A., 1968, Paleocurrents of the Late Precambrian Dickinson, W.R., and Gehrels, G.E., 2009, U-Pb ages of U1MGUz/edit ?hl =enandpli=1. to Early Ordovician (Basal Sauk) transgressive clastics detrital zircons in Jurassic eolian and associated sand- Hoffman, P.F., 1989, Precambrian geology and tectonic his- of the western and northern United States with a review stones of the Colorado Plateau: Evidence for trans- tory of North America, in Bally, A.W., and Palmer, of the stratigraphy [Ph.D. thesis]: Salt Lake City, Uni- conti nental dispersal and intraregional recycling of A.R., eds., The Geology of North America—An Over- versity of Utah, 276 p. sediment: Geological Society of America Bulletin, view: Boulder, Colorado, Geological Society of Amer- Sloss, L.L., 1963, Sequences in the cratonic interior of North v. 121, p. 408–433, doi: 10 .1130 /B26406 .1 . ica, Geology of North America, v. A, p. 447–512. America: Geological Society of America Bulletin, Dickinson, W.R., and Lawton, T.F., 2001, Carboniferous Hotz, P.E., and Willden, P., 1964, Geology and mineral v. 74, p. 93–114, doi: 10 .1130 /0016 -7606 (1963)74 [93: to Cretaceous assembly and fragmentation of Mex- deposits of the Osgood Mountains quadrangle, Hum- SITCIO]2.0 .CO;2 . ico: Geological Society of America Bulletin, v. 113, boldt County, Nevada: U.S. Geological Survey Profes- Sloss, L.L., 1988, Tectonic evolution of the craton in p. 1142–1160, doi: 10 .1130 /0016 -7606 (2001)113 sional Paper 431, 127 p., scale 1:62,500. Phanero zoic time, in Sloss, L.L., ed., Sedimentary <1142: CTCAAF>2.0 .CO;2 . Johnston, S., Gehrels, G., Valencia, V., and Ruiz, J., 2009, Cover—North American Craton: U.S.: Boulder, Colo- Erickson, R.L., and Marsh, S.P., 1974, Geologic map of Small-volume U-Pb geochronology by laser abla- rado, Geological Society of America, Geology of the Golconda quadrangle, Humboldt County, Nevada: tion–multicollector–ICP mass spectrometry: Chemical North America, v. D-2, p. 25–34. U.S. Geological Survey Geologic Quadrangle Map Geology, v. 259, p. 218–229, doi:10 .1016 /j .chemgeo Stewart, J.H., 1972, Initial deposits in the Cordilleran geo- GQ-1174, scale 1:24,000. .2008 .11 .004 . syncline: Evidence of a late Precambrian (<850 m.y.) Ferguson, H.G., Roberts, R.J., and Muller, S.W., 1952, Keith, A., 1928, Structural symmetry in North America: continental separation: Geological Society of America Geology of the Golconda quadrangle, Nevada: U.S. Geological Society of America Bulletin, v. 39, p. 321– Bulletin, v. 83, p. 1345–1360, doi:10 .1130 /0016 -7606 Geological Survey Geologic Quadrangle Map GQ-15, 386, doi: 10 .1130 /GSAB -39 -321 . (1972)83 [1345: IDITCG]2.0 .CO;2 . scale 1:125,000. Kingsbury-Stewart, E.M., Osterhout, S.L., Link, P.K., and Stewart, J.H., 1991, Latest Proterozoic and Cambrian rocks Gehrels, G.E., 2000, Introduction to detrital zircon studies Dehler, C.M., 2013, Sequence stratigraphy and for- of the western United States—An overview, in Cooper , of Paleozoic and Triassic strata in western Nevada and malization of the Middle Uinta Mountain Group (Neo- J.D., and Stevens, C.H., eds., Paleozoic Paleogeog- northern California, in Soreghan, M.J., and Gehrels, proterozoic), central Uinta Mountains, Utah: A closer raphy of the Western United States—II: Pacifi c Sec- G.E., eds., Paleozoic and Triassic Paleogeography and look at the western Laurentian seaway at ca. 750 Ma: tion, Society of Economic Paleontologists and Min- Tectonics of Western Nevada and Northern California: Precambrian Research, v. 236, p. 65–84, doi: 10 .1016 /j eralogists Paleozoic Paleogeography Symposium 2, Geological Society of America Special Paper 347, .precamres.2013 .06 .015 . p. 13–38. p. 1–17, doi: 10 .1130 /0 -8137 -2347 -7 .1 . Lawton, T.F., Hunt, G.J., and Gehrels, G.E., 2010, Detrital Stewart, J.H., Gehrels, G.E., Barth, A.P., Link, P.K., Gehrels, G.E., 2012, Detrital zircon U-Pb geochronology: zircon record of thrust belt unroofi ng in lower Creta- Christie-Blick, N., and Wrucke, C.T., 2001, Detrital Current methods and new opportunities, in Busby, C., ceous synorogenic conglomerates, central Utah: Geol- zircon provenance of Mesoproterozoic to Cambrian and Azor, A., eds., Tectonics of Sedimentary Basins: ogy, v. 38, p. 463–466, doi: 10 .1130 /G30684 .1 . arenites in the western United States and northwest- Recent Advances: Hoboken, New Jersey, Blackwell Madden-McGuire, D., 1991, Stratigraphy of the limestone- ern Mexico: Geological Society of America Bul- Publishing, doi: 10 .1002 /9781444347166 .ch2 . bearing part of the lower Cambrian to lower Ordovi- letin, v. 113, p. 1343–1356, doi: 10 .1130 /0016 -7606 Gehrels, G.E., and Dickinson, W.R., 1995, Detrital zircon cian Preble Formation near its type locality, Humboldt (2001)113 <1343: DZPOMT>2.0 .CO;2 . provenance of Cambrian to Triassic miogeoclinal and County, north-central Nevada, in Raines, G.L., et al., Van Schmus, W.R., Bickford, M.E., Sims, P.K., Anderson, eugeoclinal strata in Nevada: American Journal of Sci- eds., Geology and Ore Deposits of the Great Basin: J.L., Shearer, C.K., and Treves, S.B., 1993, Proterozoic ence, v. 295, p. 18–48, doi: 10 .2475 /ajs .295 .1 .18 . Reno, Geological Society of Nevada, p. 875–839. geology of the western midcontinent region, in Reed, Gehrels, G.E., and Pecha, M., 2014, Detrital zircon U-Pb Mueller, P.A., Foster, D.A., Mogk, D.W., Wooden, J.L., J.C., et al., eds., Precambrian: Conterminous U.S.: geochronology and Hf isotope geochemistry of Paleo- Kamenov, G.D., and Vogl, J.J., 2007, Detrital mineral Boulder, Colorado, Geological Society of America, zoic and Triassic passive margin strata of western chronology of the Uinta Mountain Group: Implica- Geology of North America, v. C-2, p. 239–259. North America: Geosphere, v. 10, p. 49–65, doi: 10 tions for the Grenville fl ood in southwestern Laurentia: Yonkee, W.A., Dehler, C.D., Link, P.K., Balgord, E.A., .1130 /GES00889 .1 . Geology, v. 35, p. 431–434, doi: 10 .1130 /G23148A .1 . Keeley, J.A., Hayes, D.S., Wells, M.L., Fanning, Gehrels, G.E., Valencia, V., and Pullen, A., 2006, Detrital Poole, F.G., Stewart, J.H., Palmer, A.R., Sandberg, C.A., C.M., and Johnston, S.M., 2014, Tectono-stratigraphic zircon geochronology by laser-ablation multi collec- Madrid, R.A., Ross, R.J., Jr., Hintze, L.F., Miller, framework of Neoproterozoic to Cambrian strata, tor ICPMS at the Arizona LaserChron Center, in M.M., and Wrucke, C.T., 1992, Latest Precambrian west-central U.S.: Protracted rifting, glaciation, and Lozweski , T., and Huff, W., eds., Geochronology: to latest Devonian time; development of a continental evolution of the North American Cordilleran margin: Emerging Opportunities: Paleontology Society Papers margin, in Burchfi el, B.C., et al., eds., The Cordilleran Earth-Science Reviews, v. 136, p. 59–95, doi:10 .1016 /j Volume 12, p. 67–77. Orogen: Conterminous U.S.: Boulder, Colorado, Geo- .earscirev .2014 .05 .004 .

1410 Geosphere, December 2014

Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/10/6/1402/3338869/1402.pdf by guest on 28 September 2021