Early Cretaceous Construction of a Structural Culmination, Eureka, Nevada, U.S.A.: Implications for Out-Of- Sequence Deformation in the Sevier Hinterland

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Early Cretaceous construction of a structural culmination, Eureka, Nevada, U.S.A.: Implications for out-of- sequence deformation in the Sevier hinterland

Sean P. Long1,*, Christopher D. Henry1, John L. Muntean1, Gary P. Edmondo2, and Elizabeth J. Cassel3 1Nevada Bureau of Mines and Geology, Mail Stop 178, University of Nevada, Reno, Nevada 89557, USA 2Timberline Resources Corporation, 101 East Lakeside, Coeur D’Alene, Idaho 83814, USA 3Department of Geological Sciences, University of Idaho, P.O. Box 443022, Moscow, Idaho 83844, USA

ABSTRACT can be traced for ~100 km north-south on the 1968; Burchfi el and Davis, 1975; Oldow et al., basis of Paleogene erosion levels. The culmi- 1989; Allmendinger, 1992; Burchfi el et al., Assessing temporal relationships between nation is interpreted as a fault-bend fold that 1992; DeCelles, 2004; Dickinson, 2004). In foreland and hinterland deformation in fold- formed from ~9 km of eastward displace- the western interior United States, major com- thrust belts is critical to understanding the ment of the Ratto Canyon thrust sheet over a ponents of the Cordillera include the Sierra dynamics of orogenic systems. In the western buried footwall ramp. Nevada magmatic arc in California, and a broad U.S. Cordillera, the central Nevada thrust belt The type exposure of the Early Cretaceous retroarc region across Nevada and western Utah (CNTB) has been interpreted as a hinterland (Aptian) Newark Canyon Formation (NCF) in which most crustal shortening was accom- component of the Sevier fold-thrust belt in is preserved on top of Mississippian, Penn- modated (Fig. 1). The retroarc region has been Utah. However, imprecise timing constraints sylvanian, and Permian rocks on the eastern divided into distinct tectonic zones, including on CNTB deformation have hindered evalu- limb of the Eureka culmination. We propose the Jurassic Luning-Fencemaker thrust belt in ation of space-time patterns of strain par- that the NCF was deposited in a piggyback western Nevada (e.g., Oldow, 1983, 1984; Wyld, titioning between these two thrust systems. basin on the eastern limb of the culmina- 2002) and the Cretaceous frontal Sevier thrust To address this problem, new 1:24,000-scale tion as it grew, which is consistent with belt in Utah (e.g., Armstrong, 1968; Burchfi el geologic mapping and balanced cross sec- published east-directed paleocurrents and and Davis, 1975; Royse et al., 1975; Villien tions are presented through the CNTB near provenance data suggesting derivation from and Kligfi eld, 1986; DeCelles and Coogan, Eureka, Nevada, in conjunction with industry proximal late Paleozoic subcrop units. Syn- 2006). Between these two loci of Cordilleran drill-hole data, conodont age determinations, contractional deposition of the NCF is used crustal shortening is a broad hinterland region and 40Ar/39Ar and U-Pb ages from volcanic, to defi ne the probable Aptian construction of that underwent distinct Jurassic and Cretaceous intrusive, and sedimentary rocks. the Eureka culmination and associated slip magmatic, metamorphic, and shortening events, Our mapping redefi nes the fi rst-order on the Ratto Canyon thrust at depth. After although the timing and relative magnitude of structures and deformation geometry of the deposition, the NCF continued to be folded Jurassic versus Cretaceous deformation within CNTB at the latitude of Eureka. Contrac- during late-stage growth of the culmination. this region are debated (e.g., Armstrong, 1972; tional structures include two north-striking, Aptian deformation in the CNTB at Allmendinger and Jordan, 1981; Gans and east-vergent thrust faults, the Prospect Moun- Eureka postdated migration of the Sevier Miller, 1983; Miller et al., 1988; Speed et al., tain thrust and Moritz-Nager thrust, which thrust front into Utah by at least ~10 m.y. and 1988; Thorman et al., 1991, 1992; Bjerrum are connected as the same fault in cross sec- possibly as much as ~30 m.y., and therefore and Dorsey, 1995; Miller and Hoisch, 1995; tion, several north-striking map-scale folds, represents out-of-sequence hinterland defor- Camilleri and Chamberlain, 1997; Taylor et al., and a Cambrian over Silurian relationship mation. CNTB deformation was coeval with 2000; Wyld et al., 2001; Martin et al., 2010; observed in multiple drill holes, correspond- emplacement of the Canyon Range thrust Greene, 2014). ing to repetition of ~2–2.5 km of stratigraphy, sheet in the type-Sevier thrust belt in western One debate centers on the timing of deforma- that defi nes the blind Ratto Canyon thrust. Utah, and may represent internal shortening tion in the central Nevada thrust belt (CNTB), Two distinct sets of normal faults cut the con- of this orogen-scale thrust sheet that acted to defi ned by Taylor et al. (1993) as a series of tractional structures, and are overlapped by a promote further eastward translation. dominantly east-vergent thrust faults and folds regional late Eocene (ca. 37 Ma) subvolcanic exposed between the towns of Alamo and unconformity. Retrodeformation of both sets INTRODUCTION Eureka, Nevada (Fig. 1). Thrust systems in the of normal faults reveals the existence of the southern part of the CNTB connect southward Eureka culmination, a 20-km-wide, 4.5-km- The Jurassic–Paleogene North American with thrust faults of the Sevier belt in southern tall anticline with limb dips of 25°–35°, that Cordillera is the type example of an ancient Nevada (Bartley and Gleason, 1990; Armstrong orogen that formed between converging con- and Bartley, 1993; Taylor et al., 1993, 2000; *Corresponding author: splong@ unr .edu tinental and oceanic plates (e.g., Armstrong, Long, 2012), implying an overlap in deforma-

Geosphere; June 2014; v. 10; no. 3; p. 564–584; doi:10.1130/GES00997.1; 13 ﬁ gures; 1 table; 3 plates; 1 supplemental ﬁ le. Received 24 October 2013 ♦ Revision received 25 February 2014 ♦ Accepted 8 April 2014 ♦ Published online 25 April 2014

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Idaho age determinations, and U-Pb and 40Ar/39Ar 120° Nevada 117° 114° 111° geochronology of volcanic, intrusive, and sedimentary rocks. These data facilitate redeﬁ nition RMT Salt of the ﬁ rst-order structures that compose the GT Lake Wyoming Elko City 41° CNTB, and reconstruction of the regional pre- Utah extensional deformation geometry. In addition, a Area of structural model is presented that relates deposi- Fig. 2 tion in the type-NCF basin to CNTB deforma- Reno Sevier fold- tion, including growth of a regional-scale anti- LFTB Eureka thrust belt cline and associated motion on a thrust fault at Austin Ely depth, thereby placing the CNTB and NCF into

Sevier

region 39° the broader spatiotemporal framework of Sevier hinterland deformation and synorogenic deposition. This cross-section line work is aided by recent U-Pb geochronology in Sierra Nevada magmatic arc CNTB of DeCelles and the NCF type section (Druschke et al., 2011) and Tonopah Coogan (2006) a recent synthesis of the timing and magnitude of crustal shortening accommodated in the type- Alamo Cedar Sevier thrust belt at the latitude of our study area City (DeCelles and Coogan, 2006), both of which 37° facilitate assessment of temporal relationships Arizona between foreland and hinterland shortening. Las Vegas Implications of this work for the dynamics of the Cordilleran orogenic wedge are then explored.

050100 150 200 N GEOLOGIC SETTING AND ESTB STRATIGRAPHY California scale (km) Eastern Nevada has occupied a diverse range Figure 1. Map showing Paleozoic and Mesozoic thrust systems of Nevada, Utah, and south- of tectonic settings that have evolved through east California (modiﬁ ed from Long, 2012). Approximate deformation fronts of Paleozoic the Phanerozoic (e.g., Dickinson, 2006). In the and Mesozoic thrust systems are shown in brown and blue, respectively, and spatial extents study area this tectonic development is pre- are shaded. Location of Sierra Nevada magmatic arc is from Van Buer et al. (2009) and served in a rock record that spans the Paleozoic, DeCelles (2004). Abbreviations: GT—Golconda thrust; RMT—Roberts Mountains thrust; Mesozoic, and Tertiary (Plate 1; Fig. 3). LFTB—Luning-Fencemaker thrust belt; CNTB—central Nevada thrust belt; ESTB—East- ern Sierra thrust belt. Paleozoic

tion timing between these two thrust systems. (Nolan et al., 1971, 1974; Hose, 1983; Vander- From the late Neoproterozoic to the Devo- However, on the basis of crosscutting relation- voort and Schmitt, 1990) (Fig. 2). Contractional nian, the Cordilleran passive margin sequence, a ships, southern CNTB thrust faults can only be deformation in the Eureka region has been pro- westward-thickening section of clastic and car- broadly bracketed between the Pennsylvanian posed to be bracketed between the Permian and bonate rocks, was deposited on the rifted North and the Late Cretaceous (Taylor et al., 2000), Early Cretaceous (Nolan, 1962; Taylor et al., American continental shelf in what is now east- hindering evaluation of space-time patterns of 1993; Lisenbee et al., 1995), to be dominantly ern Nevada and western Utah (e.g., Stewart and strain partitioning between the CNTB and the Early Cretaceous, coeval with deposition of the Poole, 1974). Eureka was situated near the dis- Sevier thrust belt. NCF (Vandervoort and Schmitt, 1990; Carpen- tal, western margin of the shelf (Cook and Cor- This problem is compounded in the north- ter et al., 1993; Ransom and Hansen, 1993), boy, 2004). In the study area the exposed part ern part of the CNTB, near the town of Eureka and possibly to be as young as Late Creta- of the passive margin sequence is 4.7 km thick, (Fig. 1), an area that has been interpreted as ceous (Vandervoort and Schmitt, 1990; Taylor and consists of lower Cambrian clastic rocks, occupying a zone of thrust faults and folds in et al., 1993). These varying interpretations are including the Prospect Mountain Quartzite, and several generations of studies (e.g., Nolan et al., further compounded by complex, overprinting a middle Cambrian to Devonian section domi- 1971, 1974; Taylor et al., 1993; Carpenter et al., extensional deformation, which has hindered nated by limestone and dolomite, with lesser 1993). Here dating of contractional deformation reconstruction of the preextensional structural quartzite and shale (Fig. 3) (e.g., Palmer, 1960; has been hindered by varying interpretations geometry. Nolan, 1962; Ross, 1970; Nolan et al., 1974). of the style and geometry of large-offset faults The purpose of this paper is to present a new During the Mississippian, the Roberts Moun- (e.g., Nolan, 1962; Nolan et al., 1971, 1974; structural and geometric deﬁ nition of the CNTB tains allochthon, composed of distal slope and Roeder, 1989; Carpenter et al., 1993; Ransom at the latitude of Eureka. To achieve this goal, a basinal sediments, was thrust to the east over and Hansen, 1993; Taylor et al., 1993; Lisenbee new 1:24,000-scale geologic map of the north- the western edge of the continental shelf dur- et al., 1995; Lisenbee, 2001a) and their relation- ern Fish Creek Range and southern Diamond ing the Antler orogeny (e.g., Burchﬁ el and ships to the Early Cretaceous Newark Canyon Mountains is presented (Plate 1; Fig. 2), along Davis, 1975; Dickinson, 1977; Speed and Sleep, Formation (NCF), a sedimentary unit preserved with deformed and restored cross sections 1982). Eureka is immediately to the east of the in several isolated exposures in the region (Plates 1–3), industry drill-hole data, conodont Antler thrust front (Fig. 1), but was the site of

Geosphere, June 2014 565

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40°N intrusive volcanic sedimentary 116°W Map units: Bald Mountain A rocks rocks rocks Holocene

Pleistocene undiff.

Roberts Diamond Mts. Pliocene breccia Mountains Miocene Oligocene Cenozoic Eocene

Sulphur Springs Range Paleocene includes Cretaceous Sheep Pass Fm. Diamond Valley Jurassic Newark Triassic Canyon

Mesozoic Long Valley Fm. Permian Pennsylvanian Lone type-section Mississippian of Newark

Mtn. Devonian Butte Mountains Canyon Fm. Newark Vly. Silurian

area of Paleozoic

Figure 2. (A) Geologic map of Fig. 10 Ordovician allochthon Eureka Roberts Mts. part of east-central Nevada; U.S. Hwy. 50 Cambrian geology simpliﬁ ed from Craf- area of ford (2007) and Quaternary Mtn. Plate 1 faults simpliﬁ ed from the U.S. Boy R. Geological Survey (2006) fault and fold database. Vly.—val- Mahogany Hills ley; R—range; Mts.—mountains; undiff—undifferenti-

ated. (B) Simplified version White Pine Range of Plate 1 with the same map units as A, showing geographic Antelope Valley names relevant to discussion in text, locations of structures,

and cross-section lines. Red Fish Creek Range dots with arrows show location and view direction of annotated photographs in Figure 7,

and blue dots show locations of Duckwater Hills 40 39 U-Pb and Ar/ Ar samples. Fish Creek Valley Pancake Range

Scale: N 0510 kilometers

Antelope Range 116°W 39°N Upper Reese Lower Reese White Dugout Prospect Hoosac Pinto Sentinel Moritz- Pinto B and Berry and Berry Mountain tunnel Mountain fault Summit Mountain Nager Creek detachment detachment anticline fault thrust system fault syncline thrust syncline

A’ A H12-78 Fig. 6 7D H10-62 Spring Valley Prospect H11-88 Peak Hoosac 7A

Rocky Cnyn. Mtn. B White B’ NMC N11DZ- Secret Canyon N Mtn. 609C

017EU 50 Hwy. Spring Valley Reese and Berry H11-86 Scale: Lookout H11- 1 km Mtn. 138 Cn 39°25’N Fig. 5 yn 7C 7B . DD’H11-92 C C’ 116°5’W Lookout Mountain fault 116°0’W Fig. 9 115°55’W 115°50’W

566 Geosphere, June 2014

Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/10/3/564/3333888/564.pdf by guest on 02 October 2021 Construction of a structural culmination, Eureka, Nevada mile feet kilometer Apparent Dip, In Cross Section Cross In Dip, Apparent Overturned Apparent Dip, In Cross Section Cross In Dip, Apparent 00.51 Scale 1:24,000 Scale 40 OR 20 FEET INTERVAL CONTOUR 0 10002000300040005000 00.51 Projection: Universal Transverse Mercator, Zone 11, 11, Zone Mercator, Transverse Universal Projection: 1927 (m) Datum American North Summit Valley Spring Survey Geological map: U.S. Base 1990) edition (Provisional quadrangle 7.5' 1990) edition (Provisional quadrangle 7.5' Summit Pinto 1990) edition (Provisional quadrangle 7.5' Mountain Silverado 37 s Apparent Dip, In Cross Section Cross In Dip, Apparent 1 10 Overturned Overturned Horizontal 37 37 e 1 s s 35 89 13 15 7 4 1 2 3 Adjoining 7.5' Overturned Vertical 1 quadrangle names 12 4 6 11 12 14 1 Hay Ranch 2 Devon Peak 3 Eureka 4 Diamond Peak 5 West of Beck Pass Combs6 Peak Spring7 SummitValley 8 Pinto Summit Mountain 9 Silverado Pancake10 Summit West of Bellvue11 Peak 12 Bellvue Peak 13 Pinto Summit SW Black14 Point Pancake15 Summit SW 37

s v v v Inclined Inclined Vertical Inclined Inclined Inclined Vertical Inclined Inclined H22-39 NMC609C ! ! 41 41 41 41 41 41 41 From the authors. 1962,Nolan, TheT.B., Eureka Mining District, Nevada: U.S. Geological Survey Professional Paper 406, 78 p. Nolan, Merriam,T.B., C.W., and Blake, M.C., Jr., 1974, Geologic map of the Pinto Summit quadrangle, Eureka Survey Geological U.S. Nevada: counties, Pine White and Miscellaneous Investigations Series, Map I-793: plates. 2 p., 14 1:31,680-scale, From Timberline Resources Corporation. o o o o 2 Â ¦ ³ 3 4 1 Sample point Drill hole Drill Strike and dip of bedding Strike and dip of bedding Strike and dip of igneous foliation Strike and dip foliationof in ash-flow tuff Strike and dip of bedding Strike and dip of bedding Strike and dip of joints Symbology

( 15º 00' × MN ((

× ^ × (( GN ( (( 0º 40' UTMAND GRID ( 1990 MAGNETIC NORTH (( Solid where certain and location accurate, long-dashed long-dashed accurate, location and certain where Solid DECLINATION AT CENTER OF SHEET OF CENTER AT DECLINATION ( (( Solid where certain and location accurate. location and certain where Solid Solid where certain and location accurate, long-dashed ( Solid where certain and location accurate, long-dashed long-dashed accurate, location and certain where Solid Boundary of Open Pit Mine Pit Open of Boundary Solid where certain and location accurate, long-dashed long-dashed accurate, location and certain where Solid Solid where certain and location accurate, long-dashed long-dashed accurate, location and certain where Solid Solid where certain and location accurate, long-dashed long-dashed accurate, location and certain where Solid

(( G ² K F % 35 : Line of cross section ( (( AA' Syncline where approximate, dotted where concealed. Contact where approximate, dotted where concealed, showing dip bearing. Internal contact Anticline where approximate, dotted where concealed. Normal Fault Normal where approximate, dotted where concealed. Ball observer. on from downthrown x away side. observer, towards dot section, cross In Thrust fault where approximate, dotted where concealed. Detachment fault where approximate, dotted where concealed. Geologic data from Nolan et al. 1974 shown in gray. 39°25'0"N 39°27'30"N 63 62 64 66 65 68 67 Qf C' B' A' Qa Mc 23 Mc 9 Qc 61 Mc Mc Mc 8 Qc 7 Mc 25 Trt Tps 02 Mdp 70 Qc 6 Qa Mdp Trt 15 02 Qf 60 Doc Tmh Tps Qf 43 Mdp 7 10 7 30 12 Knc Doc Mdp 8 27 Knc Knc Knc Knc 15 IPMe Knc Qc E Tc rm Tnh Qc Mdp 000m. 97 QTg Knc 97 Dbs Qc Tmh Ddgm Ddgm 5 22 Doc 61 Tc rm 19 Tc rm Qf Qc 19 45 Qa 25 Mdp 115°52'30"W 21 Dw Trt Mdp 18 Tps 9 17 36 Dbs Tmc 23 18 Qc Tmh 18 Qa 13 115°52'30"W 24 01 24 Ddghc 25 10 22 01 Trt 20 Ddghc 23 Qf Qf 23 24 Qf Trt Trt Qa Trt Tps Qf Qc Qc Qc Trt Trt Trt 115°50'0"W 115°50'0"W Qf Qf 40 28 19 00 Mdc Trt? 6 41 24 00 6 40 Qf Qf 40 Qf Qa Mc Mdp Doc 33 38 Mc Mc Qf Tc rm 35 99 Mc Mdp 99 Mc Qf Trt Trt Mdp 20 Trt Trt Qf Ddghc 10 Mc Qf Trma 70 Qa 80 90 71 Qa 85 49 Mdc Trt Mc 45 39 20 Qf Mdp 46 Ddghc 78 Mdp 51 Qc 24 Mc Qa 98 18 Tc rm 98 83 58 Qf Tc rm 53 0 Mj Ddghc Mdc Qf 44 Doc 75 Ddghc Trt Dbp Qc Mdc Mdp Trt 45 Trt 0 Qc MDp 65 10 13 Doc Trma 35 Qc 71 60 28 Tps 53 Tps Mc 70 12 Qc rust Tpc Nager Th 71 tz MDp Mj ri 17 Mo 75 Trt Ddghc Trt 25 Qc 7 Mc Ddghc 50 Mdc Dbp Mc Tps 60 Trt Qa Dbp 66 16 55 Dbs Doc Qc Mc 81 Mdc 11 30 Trt Trma 37 Mc 52 39°22'30"N 55 27 59 19 Dbs Mdc Dsm 19 Mdc Mc Qc Doc 97 17 Mc Trt 21 Dbp Dbs 5 97 12 9 40 30 26 Dw 20 Trt 40 Qc 21 55 60 12 25 Doc 42

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Slm a 68 Tc rm mit F Trt um Dbpq S Dbpq Pinto 21 8 Qf Tc rm Qf Trt 92 Tprt Trt Trsd 21 85 82 41 92 7 71 Dbpq 63 Slm 25 Tpr Trt 50 Qf 90 Trt 0 35 80 Pcr Trsv Pcr Qf 8 11 Trsd Qf Tprt Qf 30 5 24 Tprt Pcr Tprt 26 70 Qf Pcrc Qf Pcr 25 80 Tprt 26 Ts c Qf 25 76 Tprt 20 Tc l 19 34 Trsv 39 Tgv Trsv Tprx Pcr Trsv 74 Qa Qc Trsp Tc rm 38 Pcr 43 9 Trsp Mdp Trst Trsp Qa Trsp 42 Tc l Pcr 58 Trt 23 Trsv 39 Tprd Tgm 59 Trsp 60 Tc l Tc l 13 Qa Trsv 48 61 62 Tprt Tgv 43 H11-86 Qf Tc l Mdp Tprt Tprd Mc Qa Pcr Trsv 62 59 62 Qf 91 50 58 Tc rm 72 36 61 Mdp 61 Tpr 73 29 Tprd 58 91 21 61 34 Trsp 57 Qf 48 80 Mc 78 25 Tgm Pcr Trsp Tprd Tc l 50 12 75 Trt 77 Tprd Pcr 58 8 Trsv 31 Tprd 74 Qa 71 62 67 78 19 Mdp 51 8 Pcrc 15 13 Tprd Tgv 80 H11-88 81 77 Mc 61 64 25 70 19 41 33 Mc 59 21 64 73 Ttrf Qf Tprd 26 85 80 61 72 54 89 Mdp 40 86 46 Mdp Mc ed from Long et al. (2012). Translucent areas above modern erosion surface on cross surface on cross above modern erosion areas Translucent Long et al. (2012). ed from Qa 45 89 78 35 73 74 Mc Mc 31 Mc Pcr Tgv Qf 74 Ttrd Tgm 53 17 10 71 Tprd Tprt Qf 26 Mc Trsv? Qf Trsv Ttrf 64 53 87 Trsv? 41 35 85 Mc 58 Trsv? Tprt 25 70 48 69 89 22 60 70 90 9 31 75 90 Tprt 75 Trsv? 88 60 5 60 52 32 66 90 90 Qc 48 Ttr Tpr 5 28 Tprf 90 Trd 41 46 44 45 51 KA AND WHITE PINE COUNTIES, NEVADA COUNTIES, PINE WHITE AND KA Ts 56

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r 11

Db p 35 26

26 Ohc S 47 37 30 42 21 33 9 40 Ohc 53 12 Qc Dsr 5 42 Ohc 13 37 Dbp 46 Db Ohc Qf 13 39 30 16 Qc Qc Doc 44 Oe 18 Ohc Slm Slm 53 58 42 10 40 Dsr 63 Qa 21 Qc 19 Ohc Oe 17 61 ment Ds Ohc h Doc 51 c Dsr ta 65 30 26 Berry De 41 Oe 11 nd a 40 13 ese

Re 15 r 42 owe 46

L Dbp 38 53 8 50 19 41 Ohc 41 32 Slm Oe 13 Oe 39 40 22 40 42 18 13 55 16 Dbp 83 23 34 Qa 16 22 22 30 17 38 37 42 22 30 Db 42 83 8 Oav Qc 8 Oav Dsr 30 24 18 Slm 36 7 38 7 Ds 22 31 19 Slm 5 43 42 29 20 42 23 13 8 26 35 8 Ohc 31 20 6 Oe 52 Ohc 42 11 22 61 Slm 58 35 9 31 Ohc 31 20 Dbp Oe 11 21 29 Slm 49 12 15 12 Slm 33 11 Ddg 21 116°2'30"W 116°2'30"W 9 Qa 10 Oe 18 21 21 32 20 24 17 Dbp 9 20 25 30 31 21 32 22 19 38 Db 18 21 Ohc 19 23 13 8 10 29 82 18 13 Slm Dsr Slm 30 82 17 22 41 Oav 18 10 22 18 8 31 Db 38 19 24 6 Db Slm 31 6 8 11 Ohc 23 22 17 Db 13 38 28 18 Dbp Qc 31 48 Qa 30 27 Dsr 41 43 8 20 25 29 Dbp 11 31 9 41 13 22 11 22 17 17 17 18 Oe 58 32 22 11 19 10 18 Qc 21 Qc 21 Qa 67 17 Db 12 22 49

t Qa 22

Qa n e 6 27 m Dsr 48 ch Qa 17 Ohc ta e Oav 18 9 Qa Qc 9 5 D 13

y 29 37 42 r Ohc 81

r Ddg e 23 B Qa 12 29

d Oav 32

n 10 38 16 10 42 Qf 81 a Dbp Ddg 10 e 36 Qf s 26 12 Ddg e 29 36

6 e 7 Oav 43

R 26 16

r Ds Ddg Ti pe 24 21 Ddg Up 18 30 27 33 18 Ddg 18 Ddg Slm 20 32 31 Oe 20 Qc 17 Qa Ddg 36 38 Oav 18 Oe 22 26 Slm 11 21 Ddg Qf 42 31 23 31 Slm 11 19 26 30 section represent eroded rock. If you are viewing the PDF of this paper or reading it ofﬂ reading or of this paper viewing the PDF If you are rock. eroded section represent to view the full-sized version of Plate 1. the full-text article on www.gsapubs.org or Plate 1. 1:24,000-scale geologic map of northern Fish Creek Range, southern Mountain Boy and Diamond Mountains, Plate 1. 1:24,000-scale geologic map of northern Fish Creek A–A cross-section 22 42 51 Ds 47 21 Oe Ddg 19 Ddg 59 28 Ohc 27 Ds 11 13 23 Qa 21 24 Qf Dsr Oe Ds 51 36 Db Mdc 19 18 9 10 Ds 36 22 30 Mdc Oe 22 21 Ddg 11 22 Slm 22 Ohc Qf 23 Qc 28 13 80 11 Qf Oe 5 Qf 11 18 39 80 22 Ddg 5 31 18 Qa 37 Ddg 19 20 29 32 37 25 Slm Oe 23 10 Ds Qa Slm 11 Qc 16 Qa 9 17 12 Qa 10 Qf Qc 8 18 21 Oe Qf 8 11 Qa 9 Oav 7 8 79 11 79 22 27 10 Qf 11 Oe 30 16 Qa 116°5'0"W 116°5'0"W 19 Qf Ki 11 Oav Oav Qc 11 10 10 11 18 Qa 18 Oav Qf 13 12 11 11 12 25 23 E 11 78 32 Qf 8 000m. 11 13 32 Qf 78 5 A B 18 C 8 Qf Qf Ddg Ddg Qf Qa Ds Qf 68 67 66 65 64 63 62 39°25'0"N 39°27'30"N

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synorogenic deposition of Mississippian clastic sediments that were sourced from the Roberts Mountains allochthon (e.g., Poole, 1974; Smith Simplified Lithologic key: A map units Map units and Ketner, 1977; Poole and Sandberg, 1977). In on Plate 3 on Plates 1-2 conglomerate the study area the Mississippian section consists of 1.5 km of conglomerate, sandstone, and shale, sandstone including the Chainman Shale and Diamond Pcrc Carbon Ridge Fm., upper Peak Formation (Fig. 3) (e.g., Brew, 1961a, 7 conglomerate (>460 m) shale 1961b, 1971; Stewart, 1962; Nolan et al., 1974). IPP During the Pennsylvanian and early Permian, Pcr Carbon Ridge Fm. (580 m) limestone eastern Nevada underwent a protracted series of deformation and erosion events recorded by IPMe Ely Limestone (≤150 m) dolomite unconformity-bound packages of carbonate and clastic rocks (e.g., Trexler et al., 2004). In the 6 Mdp Diamond Peak Fm. (365 m) study area, the Pennsylvanian–Permian section consists of 1.3 km of limestone and conglomerate, including the Ely Limestone and Carbon M Mc Chainman Shale (715 m) Ridge Formation (Fig. 3).

5 Mdc Dale Canyon Fm. (305 m) Mesozoic Mj Joana Limestone (40 m) Pilot Shale (85 m) Figure 3. (A) Stratigraphic col- MDp Across eastern Nevada and western Utah, a umn of Paleozoic rock units in Ddghc Hayes Canyon mbr. (260 m) Devil’s Gate regional unconformity places Tertiary and in limestone the study area. Column on right Ddgm Meister mbr. (85 m) some places Cretaceous rocks over Paleozoic to Dbs Bay State Dolomite mbr. (235 m) shows map unit divisions used D Triassic rocks (e.g., Armstrong, 1972; Gans and 4 Dw Woodpecker Limestone mbr. (75 m) in Plates 1 and 2, and column Dsm Sentinel Mtn. Dolomite mbr. (170 m) Nevada Miller, 1983; Long, 2012). This unconformity on left shows simplifi ed unit Doc Oxyoke Canyon Sandstone mbr. (130 m) Fm. records the net erosion that occurred during divisions used on balanced cross Dbp Beacon Peak Dolomite mbr. (190 m) Jurassic and Cretaceous deformation within the Beacon Peak mbr., basal qtzite. (≤30 m) sections in Plate 3 (Cl—lower Dbpq Sevier hinterland and Cretaceous uplift of the Cambrian, Cu—upper Cam- S Slm Silurian Lone Mountain Dolomite (395 m) hinterland that accompanied crustal thickening Ohc brian, O—Ordovician, S—Silu- thickness (km) Hanson Creek Fm. (45 m) in the frontal Sevier thrust belt (e.g., Coney and rian, D—Devonian, M—Missis- 3 Oe Eureka Quartzite (107 m) Harms, 1984; DeCelles, 2004; Long, 2012). sippian, IPP—Pennsylvanian Oav Antelope Valley Fm. (305 m) In the Eureka region, the Mesozoic section is and Permian). (B) Devonian O On Ninemile Fm. (120 m) Pogonip represented by the Early Cretaceous NCF, which Group is preserved in a series of isolated exposures in stratigraphy of Fish Creek and Og Goodwin Fm. (365 m) Mountain Boy Ranges (note: Cwc Cwb the Diamond Mountains and Fish Creek Range Bullwhacker mbr. (60 m) stratigraphic column in A Windfall Fm. (Fig. 2) (Nolan et al., 1971, 1974; Hose, 1983). 2 Catlin mbr. (55 m) shows Devonian stratigraphy of Cd Dunderberg Shale (45 m) The NCF is only exposed in the northeast corner Ch Hamburg dolomite (350 m) Diamond Mountains). Cu of the map area (Plate 1), where it overlies Mis- sissippian and Pennsylvanian rocks. However, Cs Secret Canyon Shale (305 m) the NCF type section is exposed 1–5 km north of Cg Geddes Limestone (110 m) the map area in the Diamond Mountains (Fig. 2), 1 and consists of ~500 m of conglomerate, mud- Ce Eldorado dolomite (625 m) stone, and limestone (Vandervoort, 1987). Rocks in the type section exposure are interpreted to Cl Cp Pioche Shale (70 m) record fl uvial and lacustrine deposition (Vander- voort and Schmitt, 1990). The NCF type section Cpm Prospect Mountain Quartzite (>550 m) has yielded Aptian–Albian fossil fi sh, ostra- 0 cods, and nonmarine mollusks (MacNeil, 1939; B Devonian section in Fish Creek/Mountain Boy ranges: Fouch et al., 1979). A ca. 116 Ma U-Pb zircon 1 age obtained from an air-fall tuff in the type sec- Ddg Devil’s Gate Limestone (335 m) tion defi nes an Aptian deposition age, and a ca. 122 Ma youngest U-Pb detrital zircon age popu- D Ds Simonson Dolomite mbr. (430 m) lation obtained from sandstone in the type sec- Nevada tion defi nes an Aptian maximum deposition age Doc Oxyoke Canyon Sandstone mbr. (107 m) Fm. Dsr Sadler Ranch mbr. (90 m) (Druschke et al., 2011). thickness (km) Bartine mbr. (60 m) 0 Beacon Peak Dolomite mbr. (55 m) One other rock unit of possible Mesozoic age Db Dbp in the study area is a conglomerate that unconformably overlies Ordovician, Mississippian, and Permian rocks on Hoosac Mountain (Fig. 2;

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Plate 1). Nolan et al. (1974) mapped this con- 70–73 Ma (n=3) Late Cretaceous to late Eocene conglomerate glomerate as the NCF. However, the conglom- NV11DZ-017EU (n=99) erate contains detrital zircon that have a ca. 100–115 72 Ma youngest U-Pb age population, defi ned Ma (n=31) by 3 concordant grains that overlap within error (sample NV11DZ-017EU; Fig. 4; see Supple- mental File1 for methods, concordia plots, and data from individual analyses), that defi nes a Late Cretaceous maximum depositional age (e.g., Dickinson and Gehrels, 2009). The conglomerate is overlain by late Eocene dacite, defi ning a minimum deposition age.

Tertiary (Ma)

Nevada was the site of the Great Basin ignim- Figure 4. U-Pb detrital zircon age spectrum of Late Cretaceous to late Eocene conglomerate brite fl areup, an episode of silicic volcanism that sample NV11DZ-017EU collected on Hoosac Mountain (location: 39.48535°N, 115.94587°W; swept from northeast to southwest across the Fig. 2; Plate 1). Graph is a relative probability plot, which represents the sum of probability state from the late Eocene to the early Miocene distributions from ages and corresponding errors (input errors are 2σ) for all analyses. Cre- (e.g., Coney, 1978; Armstrong and Ward, 1991; taceous age populations are labeled. Refer to Supplemental File (see footnote 1) for discus- Best and Christiansen, 1991; Henry, 2008; Best sion of methods, concordia plots, and data from individual analyses. et al., 2009). Ignimbrite fl areup rocks in the Eureka region include late Eocene silicic lavas, tuffs, shallow intrusive rocks, and associated latest Cretaceous to Eocene extensional basins The dip directions of faults were determined volcaniclastic and sedimentary rocks. Volcanic (e.g., Vandervoort and Schmitt, 1990; Potter by the interactions of fault traces with topogra- rocks are concentrated in the central and north- et al., 1995; Druschke et al., 2009a, 2009b). phy in Plate 1, and quantitative estimates of the east parts of the map area (Fig. 2; Plate 1), and dip angles of faults were determined using three- include the Pinto Peak and Target Hill rhyolite STRUCTURES AND DEFORMATION point problems on fault traces (see Table SM4 in dome systems, Ratto Springs dacite, and Rich- TIMING CONSTRAINTS the Supplemental File [see footnote 1] for sup- mond Mountain andesite. K-Ar ages of these porting data). It was assumed that the fault dip volcanic rocks range between ca. 37 and 33 Ma The Eureka area has experienced a multiphase angle estimated at the modern erosion surface (Nolan et al., 1974), and new 40Ar/39Ar dates tectonic history of contractional deformation stays the same both above and below the mod- (Table 1; see Supplemental File [see footnote 1] complexly overprinted by extensional deforma- ern erosion surface. Apparent dips of supporting for age spectra, inverse isochron plots, and data tion. Interpretations of the style, geometry, and attitude measurements were projected onto the from individual analyses) show that the oldest origin of many large-offset faults in the Fish cross sections (Plates 1 and 2), and areas of simi- volcanic rocks are 37.4 Ma (late Eocene). Creek Range and Diamond Mountains have lar apparent dip were divided into dip domains. From the Neogene to the present, much of varied widely in previous studies (e.g., Nolan Boundaries between adjacent dip domains were Nevada and western Utah has been the site et al., 1971, 1974; Carpenter et al., 1993; Ran- treated as kink surfaces (e.g., Suppe, 1983), their of regional extensional tectonism. Widespread, som and Hansen, 1993; Taylor et al., 1993; orientations determined by bisecting the inter- large-magnitude, upper crustal extension began Lisenbee, 2001b), resulting in signifi cant dis- limb angle. Division of areas of the cross sec- in the early Miocene (ca. 17.5 Ma) (e.g., Dickin- agreement over deformation geometry and tim- tions into dip domains, combined with quanti- son, 2006), and by ca. 10 Ma either transitioned ing. In the following sections, map-scale faults tative constraints on fault dip angles, allowed into, or was followed by a separate episode of, and folds are described, along with observations estimation of the cutoff angles that strata make lower magnitude extension that formed the mod- that support interpretations of their style and with faults at the modern erosion surface. All off- ern Basin and Range topography (e.g., Dickin- geometry, and fi eld relationships that bracket set estimates listed in the following for specifi c son, 2002; Colgan and Henry, 2009). However, their motion timing. These observations are used faults were measured from the 1:24,000-scale although more local in scale, evidence for pre– to support construction of three 1:24,000-scale cross sections in Plates 1 and 2, by measuring middle Miocene extension in areas of Nevada deformed cross sections (Plates 1 and 2), and the displacement of matching hanging-wall and and Utah has also been presented, including three 1:100,000-scale deformed and restored footwall cutoffs across the structure. Additional tectonic denudation of metamorphic core com- balanced cross sections (Plate 3). The balanced details on fault and fold geometry, and justifi ca- plexes (e.g., Snoke and Miller, 1988; Hodges cross sections are based on the 1:24,000-scale tions for individual decisions made in drafting and Walker, 1992; Camilleri and Chamberlain, cross sections, but with simplifi ed Paleozoic and retrodeforming the balanced cross sections 1997; McGrew et al., 2000), and development of stratigraphy (Fig. 3), and with faults with are annotated in footnotes in Plate 3. All cross <300 m of offset omitted. The top row of Plate 3 sections were drafted by hand. 1Supplemental File. Zipped fi le containing 6 sup- shows the modern, deformed geometry, and the plemental fi gures, 4 supplemental tables, supplemen- bottom row shows a partially restored geom- Contractional Structures: The CNTB tal ArcGIS fi les, and a supplemental text document. If etry, with motions on extensional faults retro- you are viewing the PDF of this paper or reading it off- line, please visit http:// dx .doi .org /10 .1130 /GES00997 deformed. Angles, line lengths, and offsets on On the eastern flank of Lookout Moun- .S1 or the full-text article on www .gsapubs .org to view faults were matched between the deformed and tain (Fig. 2; Plate 1), drilling by Timberline the Supplemental File. restored cross sections (e.g., Dahlstrom, 1969). Resources Corporation has revealed an older-

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over-younger relationship at depth, deﬁ ned by is an upright, open fold, with a western limb σ

±2 Cambrian Geddes Limestone, and locally Cam- that dips 10°–20°W and an eastern limb that brian Secret Canyon Shale, over Silurian Lone dips 20°–30°E, here named the White Mountain . Isotopic

–1 Mountain Dolomite (Fig. 5), corresponding to anticline. The fold axis is cut by several normal

yr structural repetition of ~1800–2300 m of stratig- faults (Plate 1), including the lower Reese and –10 raphy. This is interpreted as evidence for a large- Berry detachment. throw thrust fault at depth, here named the Ratto In summary, contractional structures in the

MSWD total gas Canyon thrust. The thrust has been intercepted map area include (1) two east-vergent thrust in 5 drill holes over a north-south distance of traces, the Prospect Mountain thrust and Moritz- σ 3 km, at depths between 350 and 450 m, and Nager thrust, which are connected as the same does not breach the modern erosion surface structure in the cross sections (Plate 3) on the

Ar ±2 within the map area. In addition to lithologic basis of the relative stratigraphic levels that they 36 logs of drill core, the existence of the Ratto Can- deform, similar offset magnitude (~1 km), and Ar/ 40 yon thrust is corroborated by Silurian and Ordo- a lack of any surface-breaching thrust faults K decay constant) = 5.463 x 10 40

σ vician conodont age determinations from sam- observed between their traces; (2) the Ratto (Ma) Ages pled footwall rocks (Fig. 5) (see Supplemental Canyon thrust, which is deﬁ ned by a Cambrian (total File [see footnote 1] for drill-hole lithologic logs over Silurian relationship observed in drill total λ σ logical Research Laboratory (methodology in McIntosh and conodont age determination report). holes (Fig. 5), corresponding to repetition of ±2 On Prospect Mountain (Figs. 2 and 6), a ~2–2.5 km of stratigraphy; and (3) three north- ~10°E dipping fault with ~60° hanging-wall striking, upright, open folds, the White Moun- and footwall cutoff angles exhibits a top-to- tain anticline, Sentinel Mountain syncline, and K/Ca steps isochron ±2 the-east motion sense, and places older rocks Pinto Creek syncline. The Prospect Mountain

§ over younger rocks. This fault was mapped as thrust and White Mountain anticline are cut by † Ar n 39

after Min et al. (2000); an unnamed thrust fault by Nolan (1962) and normal faults that predate late Eocene volcanism %

were concentrated from crushed, sieved samples by standard magnetic and density Nolan et al. (1974), and is here named the Pros- (see following discussion), and the Moritz- σ σ pect Mountain thrust. The thrust places Prospect Nager thrust and Sentinel Mountain syncline

±2 Mountain Quartzite, Pioche Shale, and Eldorado are overlapped by late Eocene volcanic rocks. Dolomite over Secret Canyon Shale (Fig. 6), u a e

t and has ~1.0 km of top-to-the-east displacement Normal Faults a l

p (Plate 1). The Prospect Mountain thrust is cut by several normal faults (Fig. 6; Plate 1), including Normal faults in the map area can be divided the Dugout Tunnel fault. into an older set, consisting of two oppositely Ar AGES OF VOLCANIC ROCKS Ar

(°W) ≤ 39 In the southern Diamond Mountains, the verging fault systems with low ( 20°) cutoff Longitude Ar/ ~60°W dipping Moritz-Nager thrust (French, angles to bedding, including the Hoosac fault 40

NAD27 wtd mn* ±2 1993) places Devonian rocks over Mississip- system and Reese and Berry detachment system pian rocks (Plate 1; Fig. 2), and has an estimated (Fig. 2; Plate 1), and a younger set of high dip- (°N) Latitude TABLE 1. TABLE top-to-the-east displacement between 1.0 and angle, down-to-the-west normal faults. 1.8 km (Plates 1 and 2). In its hanging wall, the The down-to-the-east Hoosac fault system Sentinel Mountain syncline (Nolan et al., 1974) (Fig. 2; Plates 1–3) is an anastomosing series of strikes parallel to the thrust trace. This upright, ~70°–90°E dipping normal faults (Table SM4 open syncline plunges 15°N and has a western in the Supplemental File [see footnote 1]) with limb that dips 20°E and an eastern limb that dips low (typically ~20°) hanging-wall and footwall –4 20°–40°W. Both the Moritz-Nager thrust and cutoff angles, and a cumulative offset of ~5 km. the axis of the Sentinel Mountain syncline are This fault system is modeled on the cross sec- overlapped by late Eocene tuff (Plate 1). tions as a series of subvertical structures (Plates Though its axis is concealed under Quater- 1–3). The easternmost, master fault of the sys- nary sediment within much of the map area, tem places Mississippian and Permian rocks K/K = 1.167 x 10

40 the Pinto Creek syncline, originally described over Ordovician rocks (Fig. 7A; Plates 1–3), by Nolan et al. (1974) immediately north of corresponding to an omission of ~2–3 km of our map area, is defi ned by outcrops of Devo- stratigraphy, and a series of subsidiary faults nian, Mississippian, and Pennsylvanian strata west of the master fault deform Ordovician on the eastern fl ank of the Diamond Moun- and late Cambrian rocks (Plate 1). The master Ar used to defi ne plateau age. Ar used to defi

39 tains, in the footwall of the Moritz-Nager thrust fault has been interpreted as a steeply east dip- (Fig. 2; Plate 1). It is an upright, open syncline ping normal fault (Hague, 1892; Nolan et al., that plunges ~17°N, and has a western limb that 1974) and a shallowly west dipping thrust fault dips 30°–60°NE and an eastern limb that dips (Nolan, 1962; Taylor et al., 1993; Lisenbee,

g 10°–20°NW. 2001b) in previous studies. However, the map n i t a NAD—North American Datum of 1927. MSWD—mean square of weighted deviates. All samples were analyzed at the New Mexico Geochrono American Datum of 1927. MSWD—mean square weighted deviates. NAD—North A north-striking anticline axis can be traced patterns of both the master fault and subsidiary e Ar = percentage of h 39 along the topographic crest of the Fish Creek faults (Plate 1), combined with multiple three- p Number of single grains used in age calculation/total number analyzed. % † § *wtd mn = weighted mean, calculated by method of Samson and Alexander (1987). *wtd mn = weighted mean, calculated by method of Samson and Note: e t and Mountain Boy Ranges (Fig. 2; Plate 1). It point problems calculated along their length Sample Rock type Mineral Location H11-86 rhyolite lava dome sanidine Pinto Peak 39.42009 115.94234 36.69 0.04 13/15 172 124 H11-88ow dacite block-and-ash fl biotite Hoosac Canyon 39.44269 115.94683 37.40 0.02 93.3 7/12 37.37 0.06 308 8 1.70 37.50 0.04 et al., 2003). Neutron fl ux monitor: Fish Canyon Tuff sanidine (FC-1). Assigned age: 28.201 Ma (Kuiper et al., 2008). Minerals sanidine (FC-1). Tuff ux monitor: Fish Canyon et al., 2003). Neutron fl Decay constants nal purity. All samples were hand-picked to fi techniques. Sanidine was leached with dilute HF to remove matrix. abundances after Steiger and Jäger (1977); S H11-92H10-62H11-138H12-78 low-Si rhyolite lava dacite volcaniclastic dacite volcaniclastic dacite volcaniclastic hornblende biotite hornblende Ratto Canyon Lookout Pit plagioclase 39.39799 Windfall Canyon Rustler Pit 115.98989 39.45139 39.41140 37.34 115.95933 115.99837 39.44545 37.14 0.26 37.28 115.97562 0.12 94.0 0.21 37.43 100.0 6/10 100.0 0.02 14/14 37.40 6/6 62.9 37.12 0.14 5/9 37.31 0.12 278 0.10 37.41 299 0.08 31 276 6 310 0.40 45 0.73 37.29 20 0.38 37.15 0.57 37.27 2.1 0.22 0.38 37.64 0.04 Single crystal

570 Geosphere, June 2014

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Long et al.

Elevation (feet) Elevation

24,000 20,000 16,000 12,000 4,000 0 -4,000 -8,000

8,000 (Table SM4 in the Supplemental File [see foot- end of map of end O IPP S Cu D East M thrust Nager Moritz- Cl C’ Cu

O note 1]), demonstrate their steep eastward dip, M

S IPP C’

D M Thickness (feet) Thickness

IPP 60040,000 36,000 24,000 20,000 16,000 12,000 8,000 4,000 0 80032,000 28,000 IPP

S which refutes the thrust fault interpretation. The M East thrust Nager IPP Moritz- IPP O

C’ easternmost two faults of the system are over- S M C’ VIII M D

D lapped by late Eocene (ca. 36–37 Ma) dacite and D S D O M IPP S S S

O rhyolite (Plate 1; Fig. 7A), and the westernmost N of map area, from mapping of Nolan et al., 1971; 1974) mapping of Nolan et al., from N of map area, VIII S O M D VII

IPP two faults are cut by a late Eocene rhyolite dike S O O Cl Cu Cu 50 O U.S. Cu Hwy tion on listric Pinto Summit fault (cross-section B-B’). Retro-deformationtion on listric Pinto of a similar VI II into Creek syncline axis is interpreted as paleo-horizontal. These fold axes define axes fold These as paleo-horizontal. syncline axis is interpreted Creek into

fault (Plate 1). In addition, an angular unconformity Pinto ocation of westernmost kinkocation of westernmost surface. Summit fault ng wall of Pinto Summit fault (with locally higher tilts [~30°] in its immediate hanging hanging Summit fault (with locally higher tilts [~30°] in its immediate ng wall of Pinto ard tilt was retro-deformed in footwall of Pinto Summit fault. tilt was retro-deformedof Pinto in footwall ard fault system fault Pinto Hoosac system Hoosac surface Summit IPP thrust IX IX Prospect d bottom Mountain

VII at the base of the Late Cretaceous to late Eocene M VI fault Cu D I system O D Hoosac S S O Cu S D conglomerate on Hoosac Mountain overlaps the 16.6 km Cu O Cu fault Tunnel 24.7 km Dugout O V Cl V fault fault Cu Cu M system Tunnel

Cl Dugout Hoosac

IPP thrust ? master Hoosac fault (Figs. 2 and 8; Plate 1). D 6 Prospect Mountain M S S D Ratto O thrust

O IPP

Canyon M ? S S Cu O 5 D M 5 The down-to-the-west Reese and Berry fault Lookout fault S Mountain M O Lookout IPP

Mountain

IPP S O IV ? undifferentiated D Ratto thrust Canyon M detachment system (Figs. 2 and 7B; Plate 1) Cambrian to Silurian rocks to Cambrian S M III Cu XI 4 consists of two ~10°–20°W dipping faults D Lower Reese and Lower Cl Berry detachment

S ? 4

Upper Reese and (Table SM4 in the Supplemental File [see foot- C Berry detachment C III fault O M system Hoosac note 1]) with hanging-wall and footwall cutoff IV X Cu IPP Upper Reese and Cl Berry detachment D Lower Reese and Lower

Berry detachment

West

No vertical exaggeration angles typically between 0° and 20°. The lower 20013,000 12,000 11,000 10,000 9,000 8,000 7,000 6,000 5,000 4,000 3,000 2,000 1,000 0

S (meters) Thickness end of map of end C

C detachment is developed along the top of the IPP M D Cu ine, please visit http:// dx .doi .org /10 S O Modern erosion surface (restored cross-sections surface only) Modern erosion (restored surface sub-volcanic erosion cross-sections only) (deformed Eocene, Late cross-sections motion on Reese and Berry only) prior to (deformed level detachment system possible erosion Lowest only) cross-section B-B’ on Hoosac Mountain (deformed conglomerate Eocene late to surfaceErosion Cretaceous Late below ~1-5 km from (projected Formation surface erosion at base of Newark Canyon of Early Cretaceous level stratigraphic Approximate X

West

No vertical exaggeration

C. 39°24’20”N

3003007,000 5,000 4,000 3,000 2,000 1,000 0 -1,000 -2,000 -3,000

6,000 Ordovician Eureka Quartzite, which forms Elevation (meters) Elevation Notes common to all cross-sections, continued: all cross-sections, to common Notes mo down-to-west on Hoosac Mountain to is attributed conglomerate Eocene late to Cretaceous IX. ~20-30° eastward tilting of Late and C-C’. cross-sections A-A’ amount of tilting is applied to reported Hills in Mahogany on map of Schalla are (1978); this supports of map area west to l rocks X. ~10-20°E dips in Devonian section kink Cambrian XI. Line connecting at its intersection basal contact with westernmost surface of lower X) and P (comment western and eastern limits of Eureka culmination. Under this interpretation, ~20° of eastward tilt was retro-deformed in hangi limits of Eureka culmination. Under this interpretation, and eastern western wall; this is corrobotated by eastward tilt of the Late Cretaceous-Early Tertiary conglomerate [comment IX]), and ~10° of eastw [comment conglomerate Tertiary Cretaceous-Early eastward tilt of the Late by wall; this is corrobotated

Erosion levels: Erosion a footwall ﬂ at that can be traced for ~5 km

Elevation (feet) Elevation

24,000 20,000 16,000 12,000 8,000 4,000 0 -4,000 -8,000

D across strike. Hanging-wall stratigraphic levels

M D end of map of end IPP East B’ M B’ are typically in Silurian dolomite, indicating a Cl Cu

D S

M (feet) Thickness

60040,000 36,000 24,000 20,000 16,000 12,000 8,000 4,000 0 80032,000 28,000 maximum stratigraphic omission of 400 m. In thrust B’ Nager Moritz- East IPP B’ thrust Nager

Moritz- addition, a bedding-parallel detachment fault M IPP M D D that bounds the base of several klippen of IPP VIII S M S Eureka Quartzite on White Mountain (Fig. 2; O D syncline Sentinel Mountain syncline Sentinel Mountain S O Cl Cu S Cu VIII O IPP Plate 1) merges to the west with the lower VII section westward to decollemont at top of Eureka quartzite, at top after decollemont section observations to westward O M stratigraphic levels they deform, and lack of surface-breaching they deform, levels thrust faults stratigraphic Cu rry detachment system above modern erosion surface. This relationship is not relationship This surface. modern erosion rry above detachment system Ramp modeled as increase in footwall cutoff angle from 30° to ~70-80°. 30° angle from cutoff Ramp in footwall modeled as increase D into Summit fault. into O o master fault above and below modern erosion surface. modern erosion and below fault above o master domain on east. of kink surface with ~20° higher dips on west. VI detachment. The upper Reese and Berry detach- fault S Pinto O 50 Summit U.S. fault Cu Hwy Pinto Summit ~20-30° hanging wall and footwall cutoff-angle relative to bedding. This is based on low This is based on low to bedding. relative cutoff-angle wall and footwall ~20-30° hanging Cu fault IPP II system Hoosac Cu M VI ment places Devonian dolomite over Silurian IX IPP Ratto thrust fault Canyon VII D system Hoosac M 17.5 km O S system D IPP

3, IX dolomite, omitting between 600 and 900 m of S I Hoosac fault O M 25.1 km Lower Reese and Lower Berry detachment O Cu IPP D S O D Prospect Mtn. thrust S V O stratigraphy. In the Mountain Boy Range, the M Cu D undifferentiated Cu IPP M D V S Cl Cambrian to Silurian rocks to Cambrian O thrust fault upper and lower detachments merge, and place Tunnel Prospect Dugout Mountain fault XI Tunnel III 2 Dugout Cu Cu D fault Tunnel Dugout ed Paleozoic stratigraphic divisions (Cl—lower Cambrian, Cu—upper Cam- Cambrian, Cu—upper ed Paleozoic stratigraphic divisions (Cl—lower M Cl

S Devonian rocks over Ordovician rocks, a strati- t, with a smaller-offset western normal fault that merges int normal fault that merges t, with a smaller-offsetwestern Lower Reese and Lower IV Berry detachment D Upper Reese and

Berry detachment graphic omission of 1200–1500 m. Cumulative III IV Cl fault

B offset estimates for the Reese and Berry detach- IPP M system Cu Hoosac O B S Lower Reese and Lower Berry detachment O X

Upper Reese and ment system are 1.5–2.6 km in the Fish Creek

D Berry detachment West No vertical exaggeration

20013,000 12,000 11,000 10,000 9,000 8,000 7,000 6,000 5,000 4,000 3,000 2,000 1,000 0

Thickness (meters) Thickness Range and 4.7 km in the Mountain Boy Range

IPP end of map of end B B D

M (Plates 1 and 2). Similar low-cutoff-angle nor- Cu S O West Cl

X O

No vertical exaggeration

3003007,000 6,000 5,000 4,000 3,000 2,000 1,000 0 -1,000 -2,000 -3,000 B. 39°26’15”N B. 8,000 Elevation (meters) Elevation mal faults have been documented in other areas Notes common to all cross-sections: to common Notes normal faul eastern simplified as one master, I. Hoosac fault system II. Hoosac fault system shown retaining a steep dip at depth because it does not breach modern erosion surface modern erosion dip at depth because it does not breach of P in footwall a steep retaining shown II. Hoosac fault system retain to in order surfacefold axes, modern erosion dip as it crosses is drafted above with a flatter III. Hoosac fault system cutting Reese and Be is shown Hoosac fault system rocks observed Permian on cross-section A. Also, of wall cutoff-angle hanging

observed, and was drafted this way solely based on Hoosac fault system having a higher cumulative offset. a higher cumulative having solely based on Hoosac fault system observed, and was drafted this way surface, modern erosion and cut down- and upper Reese Berry above with ~20-30° cutoff-angle shown detachments are Lower IV. Rangein Mountain Boy and Reese Berry Canyon. fault modeled as juxtaposition sides of a kink of opposite surface dip Tunnel with steeper Dugout ~40° change in dip across V. of ~20° listricity Summit fault modeled as combination and juxtaposition sides of opposite Pinto VI. ~40° dip change across relative magnitude, and offset Mountain connected at depth, based on similar vergence and Moritz-NagerVII. Prospect thrusts are Prospect Mountain. east of cutoff-angles Modeled wall and footwall with ~30° hanging observed their traces. between ramp. footwall motion of Moritz-Nager thrust sheet over from fold VIII. Sentinel Mountain syncline modeled as fault-bend formed of the Fish Creek and Mountain Boy Ranges Elevation (feet) Elevation

20,000 16,000 12,000 8,000 4,000 0 -4,000 -8,000 -12,000

D (Cowell, 1986; Lisenbee et al., 1995; Simonds, M IPP

East end of map of end A’ A’ IPP Cl D S Cu M

O 1997; Lisenbee, 2000). Approximately 1.5 km

Thickness (feet) Thickness

60040,000 36,000 24,000 20,000 16,000 12,000 8,000 4,000 0 80032,000 28,000 syncline S

Pinto Creek Pinto south of the map area, the lower Reese and IPP A’ A’ M thrust Nager Moritz- D

cations for individual decisions made in drafting and retrodeforming cross sections are annotated. Lower right annotated. Lower sections are cross individual decisions made in drafting and retrodeforming cations for Berry detachment is cut by dikes of porphyritic IPP S M IPP O syncline D

M granite, which are correlated with late Eocene Pinto Creek Pinto M IPP S VIII O D thrust Nager Moritz- D (34.1 ± 1.5 Ma; Marvin and Cole, 1978) granite S O Cl IPP Cu S M syncline Sentinel Mountain VIII O in the Mahogany Hills (Cowell, 1986). S D y south of cross-section line. y south of cross-section line. S VII in and out of page; Silurian section is schematically thinned on deformed syncline Sentinel Cu ne in footwall of Lookout Mountain fault. This is in part responsible for steep eastward is in part steep This for responsible Mountain fault. of Lookout ne in footwall ion on listric Pinto Summit fault. ion on listric Pinto Mountain

prised of units O and S carved off of top of footwall ramp that cuts the Ratto Canyon footwallCanyon prised of units O and S carvedramp that cuts the top of Ratto off of The younger set of normal faults in the O -section. fault VI Pinto likely has dominant oblique or strike-slip wall of this in hanging of motion. Space component Summit II O IPP fault Cu system Hoosac study area consists of three high-dip-angle M 50 U.S. Hwy fault IX Pinto D IPP fault Summit system Hoosac 17.7 km O M S VII

I (typically ~60°–70°), multiple-kilometer-throw D IPP D IX S 25.1 km O Ratto thrust Canyon VI S S III O Cu O Cu S O Cu D S (~2–4.5 km), down-to-the-west faults, includ- O thrust Prospect D Mountain Reese and Berry Cu Cu M S detachment system V Cu O Cu M IPP

Cl ing the Dugout Tunnel, Lookout Mountain, and D Cu S thrust Cl fault Prospect Mountain M Tunnel Dugout fault undifferentiated M III D Tunnel Dugout S Dugout V

1 Pinto Summit faults (Fig. 2; Plates 1–3). The O Tunnel fault Tunnel Cambrian to Silurian rocks to Cambrian O Cu Cl D IV .1130 /GES00997 .S4 or the full-text article on www.gsapubs.org to view the full-sized version of Plate 3. the full-text article on www.gsapubs.org .S4 or /GES00997 .1130 represent eroded rock. Justifi rock. eroded represent it offl reading or of this paper viewing the PDF levels. If you are shows explanation of erosion corner brian, O—Ordovician, S—Silurian, D—Devonian, M—Mississippian, IPP—Pennsylvanian and Permian; see Fig. 3), all faults with an deformed geometry, shows present-day row Top simplicity. omitted for rocks Tertiary <300 m of offset omitted. Quaternary and above modern erosion areas Translucent with motion on extensional faults retrodeformed. geometry, shows partially restored row Plate 3. 1:100,000-scale balanced cross sections, with simplifi Plate 3. 1:100,000-scale balanced cross Cu Dugout Tunnel fault places shallowly east dip- D S IV M Reese and Berry Cl Hoosac fault system detachment system XI

A ping Ordovician rocks over steeply east dip- A fault system Hoosac O M IPP Cu Cl

O ping Cambrian rocks, and has between 2500 S D Reese and Berry detachment system

No vertical exaggeration and 2900 m of offset (Plates 1 and 2). The ~40° 20013,000 12,000 11,000 10,000 9,000 8,000 7,000 6,000 5,000 4,000 3,000 2,000 1,000 0

Thickness (meters) Thickness end of map of end A IPP A change in dip angle observed across the fault is D M O Cu Cl S X O

West

No vertical exaggeration modeled as juxtaposition of opposite sides of A. 39°27’30”N 1003007,000 6,000 5,000 4,000 3,000 2,000 1,000 0 -1,000 -2,000 -4,000 -3,000 Elevation (meters) Elevation Notes for A-A’ cross-section: A-A’ Notes for immediatel detachments merge 1. Reese and Berry is simplified as one detachment fault, because upper and lower detachment system cross-section: B-B’ Notes for an east-striking fault is modeled as flat because cross-section line crosses portion of fault, which Tunnel 2. Section of Dugout flat portioncomponent of motion is likely in and out page. because dominant restoration, is leftfor purpose of empty mot down-to-west on Hoosac Mountain to is attributed conglomerate Eocene late to Cretaceous 3. ~20-30° eastward tilting of Late Moritz-Nager slip into thrust. thrust and feeds 6. Structural elevation and eastward dip of Ratto Canyon thrust could indicate emplacement of a small, younger thrust sheet com younger of a small, emplacement indicate thrust could 6. Structural elevation and eastward dip of Ratto Canyon Notes for C-C’ cross-section: C-C’ Notes for Reese and Berry surface, of motion modern erosion and based on strike likely has a component detachment projects above 4. Lower cross-section. full thickness to on restored Silurian section this. is restored show cross-section to zo in alteration ~50-100 m of breccia to dolomite of Hamburg section based on collapse 5. Upper Cambrian is thinned ~300 m here cross partially-restored full thickness to on lower, section Upper Cambrian is restored here. thrust shown dip of Ratto Canyon Plate 3 Plate a kink surface (Plate 3). The Lookout Moun-

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Figure 5. Cross sections through Lookout Lookout Mtn. DDTcbr and Tj ′ West East Mountain and Ratto Canyon, showing sub- 8200 (Ds protolith) surface relationships revealed by industry Ratto Canyon Qc Tcbr (Ch protolith) Horizontal scale (ft): drill holes (green lines). Locations of cross- 8000 0 200 400 section lines are shown in lower right inset 0 100

BH-0605 Horizontal scale (m): (D–D′ is also shown in Plate 1 and Fig. 2). Qc The Ratto Canyon thrust places Cambrian 7800 Geddes Limestone over Silurian Lone Ds Cd Cw Trsv 7600

Mountain Dolomite. Silurian and Ordovi- 2300 cian conodonts obtained from footwall rocks Ds

corroborate drill-hole lithologic interpreta- 7400 tions (see Supplemental File [see footnote 1] Lookout Cs

Mountain 2200 2400

for supporting lithologic logs and conodont 7200 fault Cd Elevation (ft)

age determinations for drill holes BH-0605 Elevation (m) and BHSE-007C).

7000 Ratto Canyon

Doc thrust 2100 Doc 6800 Cg tain fault places Devonian rocks over Cambrian Ch rocks, and has ~2000 m of down-to-the-west 6600

Slm Ch 2000 offset at Lookout Mountain (Plates 2 and 3). Dsr

The Dugout Tunnel and Lookout Mountain 6400 Ohc faults are both overlapped by the late Eocene Db

subvolcanic unconformity. In the footwall of Oe 1900 6200 the Lookout Mountain fault, the unconformity Late Ordovician No vertical Dbp is on Cambrian rocks (Plate 1; Fig. 5), while exaggeration conodonts modern erosion levels in its hanging wall pre- 6000 Tj Lookout Mtn. Horizontal scale (ft): serve Devonian rocks. In addition, 3–6 km Tj 0200400 E (Ds protolith) E′ West (Ch protolith) south of the map area, late Eocene volcanic 7800 0 100 East Cd Horizontal scale (m): Ratto Canyon rocks are mapped on both sides of the Look- Tcbr out Mountain fault (Nolan et al., 1974; Cowell, (Ds protolith) Qc

7600 E-007C 2300 1986), with Cambrian erosion levels in the foot- BHS Cd wall and Devonian erosion levels in the hang- Cd Cd

7400 Cd ing wall. In the footwall of the Dugout Tunnel Ch Tcbr fault, ~200 m south of the map area, Nolan (Cs protolith) Cd 2200

7200 Tcbr et al. (1974) mapped late Eocene rhyolite in Ds Cd (Ch protolith) depositional contact over Cambrian rocks,

while modern erosion levels in its hanging wall 7000 Lookout preserve strata as young as Ordovician (Fig. 9), Cs Ti Mountain 2100 Elevation (m) indicating that the majority of motion had to be Elevation (ft)

6800 fault pre–late Eocene. In Rocky Canyon (Fig. 2; Plate 1), the Dug- Ratto 6600 Cg

out Tunnel fault places unmetamorphosed Canyon 2000 Ordovician limestone over Cambrian Secret thrust Slm Canyon Shale that is metamorphosed to horn- 6400 Doc fels, which is interpreted as contact metamor- Ohc 1900

phism associated with intrusion of Late Creta- 6200 Early Silurian ceous granite dikes at depth. This is supported conodonts Dsr Oe Late Ordovician by drill hole NMC609C, located 600 m to the No vertical 6000 conodonts southeast (Fig. 2; Plate 1), which drilled through exaggeration 1800 Silurian and Ordovician dolomite, quartzite, and Map units: Locations: Prospect Qc - Quaternary colluvium Moritz- Mtn. limestone before abruptly intercepting Secret Nager Tcbr - Tertiary collapse breccia Dugout thrust Canyon Shale metamorphosed to hornfels and Tj - Tertiary jasperoid Tunnel Pinto thrust Lookout fault Hoosac Summit skarn. The metamorphism is spatially associ- Ti - Late Eocene(?) intrusive Mtn. fault fault fault Trsv - Late Eocene Ratto Springs volcanics system ated with numerous two-mica granite dikes Devonian Nevada Formation: Reese and Berry DD′ intercepted in the drill hole. We present a new Ds - Simonson dolomite member detachment system Doc - Oxyoke Canyon sandstone mbr. EE′ U-Pb zircon crystallization age of 86.1 ± 0.8 Ma Dsr - Sadler Ranch member Ordovician: Cambrian: (2σ) from a granite dike sampled from drill core Db - Bartine member Ohc - Hanson Creek dolomite Cw - Windfall Formation Dbp - Beacon Peak member Oe- Eureka quartzite Cd - Dunderberg shale (sample NMC609; see Supplemental File [see Slm - Silurian Lone Mtn. dolomite Ch - Hamburg dolomite footnote 1] for methods, concordia plot, and Cs - Secret Canyon shale

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A B lower thrust fault

Prospect Mountain Ce thrust

Prospect Mountain thrust: N hanging wall N 500 m footwall 500 m Map units: Location: Prospect Qc - Quaternary colluvium Moritz- Mtn. Nager Ttrd - Tertiary rhyolite dike Dugout thrust thrust Ch - Cambrian Hamburg dolomite Tunnel Pinto Lookout fault Hoosac Summit Cs - Cambrian Secret Canyon shale Mtn. fault fault fault Ce - Cambrian Eldorado dolomite system Cp - Cambrian Pioche shale Reese and Berry Cpm - Cambrian Prospect Mountain quartzite detachment system

Figure 6. (A) Geologic map of the Prospect Mountain thrust (location shown in Fig. 2 and bottom right inset). Crosscutting normal faults drop trace of thrust below modern erosion surface on east and west. (B) Map of the same area as A, with hanging wall and footwall of Prospect Mountain thrust labeled.

data from individual analyses), which overlaps SM4 in the Supplemental File [see footnote 1]), along most of its length by late Eocene volcanic within error with the 84 ± 2 Ma age obtained deﬁ ne a steep (~65°–75°) westward dip, which rocks (Plate 1). Eastward tilting accompanying by Barton (1987) from a granite dike sampled refutes the thrust fault interpretation. Offset esti- motion on the Pinto Summit fault is interpreted from the same drill hole. This indicates that the mates for the Pinto Summit fault range from 3.7 as the most likely mechanism for tilting the Late Dugout Tunnel fault cuts a contact aureole asso- to 4.5 km (Plates 1–3). The fault is overlapped Cretaceous to late Eocene conglomerate on ciated with a ca. 86 Ma intrusive system, which provides a maximum motion age. The Dugout Tunnel fault also cuts a detachment fault that bounds a klippe of Eureka Quartzite (Plate 1), Figure 7 (on following page). Annotated photographs (locations and view directions shown which is correlated with the lower Reese and in Fig. 2, unit abbreviations shown in Plate 1). Dashed lines with dip numbers are apparent Berry detachment. dip symbols. Red lines represent late Eocene unconformity. (A) Hoosac fault system viewed The Pinto Summit fault (Lisenbee, 2001b) from Hoosac Mountain. Eastern, master fault places Permian rocks over Ordovician rocks, places steeply east dipping Permian rocks on and westernmost fault omits units On and Oav. Late Eocene unconformity at base of unit the west against shallowly east dipping Silurian Trsv overlaps master fault. Qu—undifferentiated Quaternary deposits. (B) Reese and Berry rocks (Figs. 2 and 7C; Plates 1 and 2). The Pinto detachment system in Reese and Berry Canyon. Lower detachment occupies upper contact Summit fault has previously been interpreted as of Eureka Quartzite (Oe) for several kilometers across strike. Upper detachment places top a down-to-the-east normal fault (Nolan et al., of Devonian section (units Ds and Ddg) over lower Devonian rocks and Silurian rocks. Unit 1974; Lisenbee, 2001b) and a top-to-the-west Du represents map units Dbp, Db, Dsr, and Doc undifferentiated. (C) Pinto Summit fault reverse fault (Taylor et al., 1993). However, placing Permian rocks over Silurian rocks; note steeper dips in hanging wall. Late Eocene the map patterns of exposures on the north and unconformity at base of unit Ttt overlaps the fault. (D) Late Eocene unconformity at base south ends of the map area (Plate 1), combined of Pinto Peak rhyolite (Tpr) and associated breccia (Tprx) and sedimentary rocks (Ts) is with the results of three-point problems (Table negligibly tilted, and overlies 60°–70°E dipping Mississippian and Permian rocks.

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70E 80E A 73E NW N NE Cs 86E 90E ~400m Ch 83E 68E 72E 73E 90E 65E Mc 40E 31E Pcr Ch 81E Mdp Pcrc 90E Cd Og Oe Tc 31E 33E 58E Cwc 74E Trsv 36E Cd Cwb Windfall Canyon Qu 58E Trsv Qu 52E 73E 90E Oe 61E Qu Oav Hoosac Pcr fault 78E Pcrc system Oe 69E Qu Qu master fault N NE B Upper Reese and 41W Berry detachment 38W Ddg 49W Ds 20NW ~500m Ds Ddg 42W Du Du Qaf Ohc Ds 21W 21W Ddg Slm Qaf 24W Du 37W 21W 29W 30NW Slm 22W Oe 20W Slm Oe Oe 26W

Reese and BerryOav Canyon Lower Reese and Slm Oe Oe Qc Berry detachment

C S approximate scale SW on skyline (m) 0 100200 300 82E 80E 90E 68E Ttrx 46E Pcrc 76E 74E Ttt Mdp Slm Pcr Qc Qc Ttt Ttt Pcr Qc Qal U.S. Highway 50 Pinto Summit fault

D SE Pinto S ~200m Peak Tpr Tprx 42E 74E Ts Pcr 61E Mdp 70E Mc Qc 71E Trsv 64E Mdp Mc 64E Trsv Qc 78E 74E Mdp Qc Qal Mc Trsv

Figure 7.

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Hoosac FW: sures of late Eocene volcanic rocks (Plate 1), A N B N 332, 48NE indicating that these canyons must have been Hoosac HW: Late K-late Eo cgl: 342, 39NE incised by the late Eocene. 020, 32SE Geometry and Stratigraphic Level of the Early Cretaceous Unconformity

The Early Cretaceous NCF is only preserved in the northeast corner of the map area, in a series of exposures that unconformably overlie Hoosac FW: the Mississippian Diamond Peak Formation 345, 72E and Pennsylvanian Ely Limestone (Plate 1). However, the 5-km-long, semicontinuous expo- Hoosac HW: 355, 67E sure that contains the type section of the NCF is located 1–5 km north of the map area (Figs. 2 and 10), where the formation unconform- Late Cretaceous to late Eocene conglomerate (n=29) ably overlies the Mississippian Diamond Peak Ordovician rocks in footwall of master Hoosac fault (n=21) Formation, Pennsylvanian Ely Limestone, and Mississippian-Permian rocks in hanging wall of master Hoosac fault (n=24) Permian Carbon Ridge Formation (Nolan et al., 1971, 1974). Nolan et al. (1971) also mapped Figure 8. Equal-area stereonet plots (generated using Stereonet 8; Allmendinger et al., the NCF unconformably overlying the Missis- 2011). (A) Poles to planes of bedding of Ordovician rocks in footwall (FW) of master Hoosac sippian Diamond Peak Formation and Permian fault (purple), Mississippian–Permian rocks in its hanging wall (HW; red), and overlapping Carbon Ridge Formation 1–4 km north of the Late Cretaceous to late Eocene conglomerate (Late K–late Eo cgl; green). Great circles map area, at and south of the town of Eureka show median bedding orientation for all measurements. Plot defi nes angular unconformity (Fig. 2). with ~40° of differential tilt between Paleozoic rocks and conglomerate. (B) Same data as Within our map area, Nolan et al. (1974) in A, but rotated so average bedding of Late Cretaceous to late Eocene conglomerate (020°, mapped several isolated exposures of conglom- 32°SE) is restored to horizontal. Great circles for median bedding of rocks in footwall and erate and other lithologies that unconformably hanging wall of Hoosac fault are an approximation for original eastern limb dip of Eureka overlie rocks between Ordovician and Permian culmination at this locality. in age as the NCF. We have reexamined all of these exposures, and we map them as a vari- ety of different rock units, including Permian Hoosac Mountain 20°–30° to the east (Plate 1; Geometry of the Late Eocene conglomerate, Late Cretaceous to late Eocene Fig. 8). This brackets the maximum motion Subvolcanic Unconformity conglomerate, sedimentary rocks associated age on the Pinto Summit fault as ca. 72 Ma, the with late Eocene volcanism, and Quaternary col- maximum deposition age of the conglomerate. The map patterns of late Eocene volcanic luvium. Figure SM6 in the Supplemental File In addition, because the conglomerate overlaps rocks, as well as the map-scale geometry of the (see footnote 1) shows a side by side comparison the Hoosac fault system, but was likely tilted subvolcanic unconformity, indicate that only of our mapping and the mapping of Nolan et al. eastward by motion on the Pinto Summit fault, minor (≤10°) tilting or vertical throw on normal (1974), as well as fi eld photographs of outcrops, this indicates that the Hoosac fault system pre- faults has taken place in most of the map area for areas of key importance where we have dis- dates the Pinto Summit fault (Plates 1–3). since the late Eocene. For example, the ~9 km2 agreed with their mapping of the NCF. These In summary, normal faults in the map area can Pinto Peak rhyolite dome is rimmed with vol- areas include: (1) the axis of the Sentinel Moun- be divided into two distinct sets, both of which canic breccia and pyroclastic deposits that tain syncline (Fig. SM6A in the Supplemental predate late Eocene (ca. 37 Ma) volcanism: exhibit subhorizontal map patterns (Plate 1; Fig. File [see footnote 1]), where we map unconsoli- (1) an older set consisting of the down-to-the- 7D). Volcaniclastic deposits associated with the dated and locally cemented angular limestone east Hoosac fault system and down-to-the-west Ratto Springs dacite have a general ~10°SE dip, cobbles and boulders that overlie Devonian Reese and Berry detachment system, which which may partly refl ect deposition on paleo- rocks as Quaternary colluvium; (2) areas in the have low (≤20°) cutoff angles to bedding, and topography, but are capped by conglomerate footwall of the Pinto Summit fault (Fig. SM6B offset magnitudes between ~2 and 5 km; and and gravel that exhibit subhorizontal basal con- in the Supplemental File [see footnote 1]) where (2) a younger set consisting of high-dip-angle tacts and yield variable strike directions and dip we map pebble conglomerate with a white, tuffa- (60°–70°), down-to-the-west normal faults with angles typically ≤7° (Plate 1). ceous matrix that overlies Silurian rocks as con- offset magnitudes between 2 and 4.5 km, includ- The late Eocene unconformity is exposed in glomerate associated spatially and temporally ing the Dugout Tunnel, Lookout Mountain, and three or more localities on each cross section, with late Eocene volcanism, similar to other syn- Pinto Summit faults. Faults of set 1 are cut and distributed across the eastern two-thirds of volcanic conglomerate mapped near Pinto Sum- tilted by faults of set 2, and faults of set 2 cut the map area (Plates 1–3). The cross sections mit; and (3) on Hoosac Mountain (Fig. SM6C in a Late Cretaceous (ca. 86 Ma) contact aureole illustrate that the late Eocene erosion surface the Supplemental File [see footnote 1]), where and tilt conglomerate that has a Late Cretaceous mimics the modern erosion surface, and is not red matrix, limestone-clast pebble conglomerate (ca.72 Ma) maximum deposition age. Motion tilted at a regional scale (Plate 3). Notably, the that overlies Ordovician rocks in the footwall of on faults of set 2 was accompanied by as much topographic lows of several prominent canyons the Hoosac fault system, and Mississippian and as to ~20°–30° of eastward tilting. incised into Paleozoic bedrock contain expo- Permian rocks in its hanging wall, yields a Late

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Og Cs Cs Dahlstrom, 1969); (2) restoring the displace- Qu Cw ments of matching hanging-wall and footwall Oe Qu Og Ce cutoffs across all normal faults; and (3) retro- Tu Cg western- Ce most Cs deformation of ~25° of eastward tilting in the Qu Dugout Tunnel fault of hanging wall of the Pinto Summit fault, based Oe fault Hoosac on the dip of the Late Cretaceous to late Eocene system our mapping conglomerate on Hoosac Mountain. Details on Tu Cw Nolan et al. (1974) Og Og Cs additional constraints used in retrodeforming Cg Qu Og Og extension are annotated in footnotes in Plate 3. Ce Comparison of deformed and restored lengths Og Qu N reveals similar extension magnitudes for all Tu three cross sections, with a total range of 7.4– Tu Qu 500 m Og 8.1 km (~45%–50% extension). Map units: Retrodeformation of extension reveals a simi- Qu - Quaternary deposits, undiff. Cw - Cambrian Windfall Fm. lar preextensional deformation geometry on all Tu - late Eocene volcanics, undiff. Cs - Camrian Secret Canyon shale three cross sections, defi ned by an upright anti- Oe - Ordovician Eureka quartzite Cg - Cambrian Geddes limestone cline with a wavelength between 19 and 21 km Og - Ordovician Goodwin Fm. Ce - Cambrian Eldorado dolomite and an amplitude between 4.3 and 5.0 km, which is here named the Eureka culmination. The exis- Location: Prospect tence of this regional structural high is indepen- Moritz- Mtn. Nager dently corroborated by Paleogene subcrop and Dugout thrust thrust erosion patterns. In Long (2012), a paleogeo- Tunnel Pinto Lookout fault Hoosac Summit logic map of the Sevier hinterland was presented Mtn. fault fault fault system that showed the distribution of Neoproterozoic Reese and Berry to Triassic rocks exposed beneath the regional detachment system Paleogene, subvolcanic unconformity, and illus- trated the approximate map patterns of regional- scale, pre-unconformity structures. Figure 11 Figure 9. Geologic map of southern part of Secret Canyon (loca- shows a Paleogene subcrop map of the Eureka tion shown in lower inset and in Fig. 2), showing fi eld relationships region (modifi ed from Long, 2012) that reveals of late Eocene unconformity on either side of Dugout Tunnel fault. the approximate map patterns of several north- Unconformity is on Cambrian Secret Canyon Shale in footwall trending, erosionally beveled, pre-Paleogene (green arrow) and on Ordovician Goodwin Formation in hanging folds, with erosion levels typically in Mississip- wall (blue arrow). Units as high in the section as Eureka Quartzite pian to Triassic rocks. However, the Eureka cul- are locally preserved in hanging wall (red arrow). mination exhibits erosion levels as much as 4 km deeper than the folds in the surrounding ranges, and can be traced along strike for ~100 km, from Cretaceous (ca. 72 Ma) youngest detrital zircon The low structural relief of the Early Creta- the northern Pancake Range, where it exhibits population, and is therefore a distinctly younger ceous unconformity also has important implica- Ordovician subcrop levels, through the study rock unit than the NCF. tions for the maximum motion age of the Pinto area, where subcrop levels are as deep as Cam- Our new mapping and geochronology data Summit fault and Hoosac fault system, which brian, and into Diamond Valley, on the basis refute the original interpretation of Nolan et al. Nolan et al. (1974) originally mapped as being of Devonian and Mississippian subcrop levels (1974) that the NCF was deposited on strata as overlapped by the Early Cretaceous uncon- observed in drill holes. In the study area deep old as Ordovician, Silurian, and Devonian, and formity. Subcrop relationships defi ned by our subcrop levels represent a combination of ero- therefore have fundamental implications for the new mapping show that the NCF overlies simi- sional exhumation of the Eureka culmination map-scale geometry and basal structural relief lar stratigraphic levels on either side of the Pinto during and after its construction, and tectonic of the Early Cretaceous unconformity. The Summit fault, indicating that it cuts the Early exhumation by pre–late Eocene normal faulting. ages of subcrop units observed beneath NCF Cretaceous unconformity (Plate 3). Our map- exposures in the northeast part of our map area ping and geochronology data show that the NCF Structural Model (Plate 1), in the type exposure (Fig. 10) (Nolan is not preserved in the footwall of the Hoosac et al., 1971, 1974), and at and south of the town fault system, which suggests that this fault sys- In regions that have undergone superposed of Eureka (Fig. 2) (Nolan et al., 1971, 1974), tem also cuts the Early Cretaceous unconformity. contractional and extensional tectonism, one show that stratigraphic levels below the Mis- of the largest uncertainties in restoring and sissippian Diamond Peak Formation were not EUREKA CULMINATION quantifying deformation is how to differenti- breached by the Early Cretaceous. This indi- ate between the effects of tilting and folding cates that the NCF was deposited on a substrate The cross sections on the bottom row of associated with motion on normal faults versus of Mississippian to Permian rocks that had a Plate 3 were retrodeformed for extensional motion on thrust faults. In our cross sections, maximum regional structural relief of ~1.5 km, deformation, which was accomplished by: this equates to uncertainty in how to model the estimated using stratigraphic thicknesses in (1) matching line lengths and angles between relationships of kink surfaces to the geometries Figure 3. the deformed and restored cross sections (e.g., of specifi c structures at depth, because folding

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mbr 30 Knc mbr 30 QTu undifferentiated Tertiary volcanics and Knc 15 Quaternary sediment QTu 20 70 70 northern 40 Pcr mbr landslide masses (megabreccias) Pcrc composed of map unit IPMe continuation 10 60 20 of Pinto Knc Newark Canyon Formation Creek syncline 20 IPMe Pcrc Carbon Ridge Formation upper conglomerate 10 70 Pcr Carbon Ridge Formation 30 Newark Canyon road Pcr IPMe Ely limestone 27 30 Mdp Diamond Peak Formation 25 Knc 20 35 40 40 Mc Chainman shale 70 25 25 W limb, median 30 30 E limb, median 20 orientation N orientation: 356, 20W 331, 37NE 15 28 (n=18) (n=54) 37 5 17 30 50 60 20 IPMe 10 30 40 Mc 35 IPMe 60 20 55 50 N ′ 15 20 10 25 Mdp

39°30 55 Knc 20 35 35 40 30 47 65 57 30 15 17 Knc attitude Paleozoic (n=31) attitude (n=41) ? 30 25 17 Mdp 80 68 25 IPMe Knc QTu Knc 13 22 20 Mdp 10 42 58 Mdp 20 20 30 IPMe 35 20 QTu IPMe Mdp 44 42 47 IPMe 25 Knc 20 70 5 Mdp 20 Knc Knc 14 20 Knc 40 32 ? 60 80 QTu 10 10 projected trace of Mc approximate trace of Moritz-Nager thrust 65 60 Pinto Creek syncline Knc 55 Mc N 65 80 70 10 1 km 60 115°50′W 30 Mdp

Figure 10. Geologic map of part of southern Diamond Mountains, adjoining north edge of Plate 1 (location shown in Fig. 2), simpli- ﬁ ed from Nolan et al. (1971, 1974), illustrating map pattern of exposure that contains type section of Newark Canyon Formation (type section is along Newark Canyon road). Early Cretaceous unconformity is on map units Mdp, IPMe, Pcr, and Pcrc. Stereo- net plot (equal-area, generated using Stereonet 8; Allmendinger et al., 2011) shows poles to planes of bedding for Paleozoic and Cretaceous rocks, and median limb orientations of Pinto Creek syncline, based on all Paleozoic–Cretaceous attitudes in each limb.

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N 0255101520 E 116° Y Y Pc Scale (km) Y PPc Trmt Subcrop map explanation: Roberts Y Knc Early Cretaceous Mts. Y MDs Y TrmtPPcdLower Triassic 40° thrust Y Pc Upper Permian E Psc Lower Permian Y Y Dc DcPPc,PPcd Pennsylvanian Knc Psc MDs Mississippian Y MDs Y Dc Devonian Dc Y MDs Y Y Y SOc Silurian E MDs PPcdOc Ordovician PPcd E PPcd Cc Cambrian Y Butte ? Subcrop data explanation: synclin- E Eureka Subcrop beneath exposure of orium Y culmination Paleogene unconformity Dc Pc Y Youngest possible subcrop beneath Y Y Psc Paleogene unconformity E Sc Pinto E Subcrop beneath Paleogene Y Knc Summit unconformity in drill hole Knc fault Eureka Y Y Y Youngest possible subcrop beneath Hoosac Paleogene unconformity in drill hole fault Y Y ? Y Easternmost exposure of rocks in Y system Moritz- Y E hanging wall of Roberts Mountains Nager thrust Y Oc Sc thrust Ranges and valleys: Cc MDs Y Y Ruby Mts. MDs Dugout PPcd Area of Tunnel Plate 1 fault Bald Mtn. Y Psc

Diamond Range Dc ? Maverick Spr. R. Sc Dc Y Psc

Sulphur Springs R. Diamond Valley MDs Newark Valley Y Oc Pancake

Long Valley thrust Y Sc

Butte Mts. Y Area of MDs Duckwater Eureka thrust Plate 1 E Mtn. MDs Boy R. Knc Y PPc

White Pine Range Mahog. Hills U.S. 50 Dc Y Dc Y Roberts Ks Y Y Mts. thrust Moody

Fish Ck. R. Y 39° Peak Y Duckwater Hills thrust Fish Ck. Valley Y PPc Pc Pancake Range McClure Dc Dc PPc Spring MDs syncline PPcd Ks Y

Figure 11. Paleogene subcrop map of Eureka region (modiﬁ ed from Long, 2012), showing subcrop patterns of regional-scale, erosionally beveled, pre-Paleogene folds (including Eureka culmination), Newark Canyon Formation exposures, and pre–late Eocene normal faults in study area.

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can be attributed to changes in the geometry of 35°; (2) rocks as deep as the Cambrian Prospect Dolomite, and then forms a footwall fl at within nonplanar normal faults (e.g., Hamblin, 1965; Mountain Quartzite are exposed in the hanging the Silurian section toward the east (Figs. 12A, Groshong, 1989; Dula, 1991; Xiao and Suppe, wall of the Ratto Canyon thrust, indicating the 12B). The Prospect Mountain thrust is shown 1992) or thrust faults (e.g., Boyer and Elliott, highest permissible stratigraphic position for using the Ratto Canyon thrust surface along and 1982; Suppe, 1983; Mitra, 1990). Therefore, the regional basal dècollemont; (3) the Silurian west of its footwall ramp, and branching upward determining how to fi ll the space in the cross sec- Lone Mountain Dolomite is in the footwall of from the top of the footwall ramp at a ~35° cutoff tions beneath the Moritz-Nager thrust and, more the Ratto Canyon thrust under the culmination angle to strata (Figs. 12B–12C). Based on their important, beneath the structurally lower, larger crest; and (4) older-over-younger relationships similar offset sense and magnitude, the relative offset Ratto Canyon thrust, is the largest uncer- are not observed in the footwall of the Moritz- stratigraphic levels that they deform, and a lack tainty in the cross sections. This space must be Nager thrust, where strata as deep as the Devo- of any surface-breaching thrust faults observed fi lled with structurally repeated Paleozoic rocks nian Oxyoke Canyon Sandstone are exposed between their traces, the Prospect Mountain and (Plate 3), and many geometric solutions are pos- (Plate 1); therefore, all rocks exposed in the Moritz-Nager thrusts are connected as the same sible. Because the uncertainty in projection of Diamond Mountains are interpreted to be in the structure at depth (Fig. 12C; Plate 3). The Senti- kink surfaces and corresponding dip domains hanging wall of the Ratto Canyon thrust, which nel Mountain syncline is interpreted as the trail- propagates with depth, as more structures are cannot have ramped upsection through more ing axis of a fault-bend fold that formed above crossed, a simplifi ed structural model for con- than 300 m of footwall stratigraphy between a footwall ramp on the Moritz-Nager thrust tractional deformation in the study area is pre- here and its interception recorded in drill holes (Fig. 12C). sented here (Fig. 12), rather than attempting to ~10 km to the west. The 20 km wavelength and 4.5 km amplitude balance fault offsets and cutoff angles for con- The simplest structural model that explains of the Eureka culmination can be reproduced tractional structures on individual cross sections. these observations is that the Eureka culmina- with a 27° footwall ramp angle, which is an First-order observations that must be satisfi ed tion represents a fault-bend fold (e.g., Suppe, approximate average of the dips of the west- in the structural model include the following: 1983) constructed by eastward motion of the ern and eastern limbs, 9 km of displacement (1) the Eureka culmination has a wavelength Ratto Canyon thrust sheet over a footwall ramp on the Ratto Canyon thrust, and an additional of ~20 km, an amplitude of ~4.5 km, and pre- that cuts from the Cambrian Prospect Moun- 1 km of displacement on the Prospect Moun- extensional average limb dips between 25° and tain Quartzite to the Silurian Lone Mountain tain–Moritz-Nager thrust, for a total of 10 km

West approximate pre-NCF erosion level East A ? IPP ? Figure 12. Simpliﬁ ed structural M model for central Nevada thrust D belt (CNTB) deformation in S 7.5 km map area, showing construc- O Cu tion of Eureka culmination 27° Cl as a fault-bend fold (abbreviations: Cl—lower Cam- future Ratto Canyon thrust Eureka culmination future Prospect brian, Cu—upper Cambrian, erosion Mountain/Moritz- B IPP Nager thrust NCF type-section O—Ordovician, S—Silurian, piggyback basin D—Devonian, M—Mississip- M folding >500 m pian, IPP—Pennsylvanian and West D East S thick Permian; see Fig. 3). (A) Unde- O formed geometry. NCF— Cu Newark Canyon Formation. 9 km Cl (B) 9 km of eastward motion of S O Ratto Canyon thrust sheet over Cu Ratto Canyon thrust footwall ramp that cuts from Cl base of unit Cl to top of unit S, White Mtn. Sentinel Mountain syncline axis and coeval deposition and fold- Eureka culmination anticline axis 20 km Prospect Mountain/Moritz-Nager thrust ing of Newark Canyon Forma- erosion top of IPP tion (NCF) in piggyback basin IPP on eastern limb of culmination. C M folding Pinto Creek syncline axis 4.5 km (C) 1 km eastward displace- West D East ment on Prospect Mountain/ S top of IPP O Moritz-Nager thrust, shown Cu M IPP reactivating Ratto Canyon S D 1 km Cl Cl Cu O thrust along and west of foot- S wall ramp, and branching from O top of footwall ramp. Cu Cl

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of horizontal shortening (Fig. 12). Because this exposures tentative (e.g., Vandervoort, 1987; Coogan, 2006). Therefore, Aptian (ca. 116 Ma) is a simplifi ed geometric model, this shortening Carpenter et al., 1993). For example, on the growth of the Eureka culmination postdated estimate should be considered approximate. basis of biostratigraphy, rocks mapped as NCF migration of the Sevier thrust front into Utah in the Fish Creek Range can only be narrowed by at least ~10 m.y., and possibly as much as DISCUSSION between Barremian and Albian (Fouch et al., ~30 m.y., defi ning out-of-sequence hinterland 1979; Hose, 1983), and rocks mapped as NCF deformation. Relationship of Eureka Culmination in the Pinon Range and Cortez Mountains are Using a regional balanced cross section, to NCF Deposition broadly bracketed as Early to Late Cretaceous DeCelles and Coogan (2006) documented (Smith and Ketner, 1976; Fouch et al., 1979). 220 km of total shortening in the type-Sevier Fundamental questions remain regarding In addition, in the Pancake Range and northern thrust belt in western Utah, at the approximate the timing and geometric relationship of NCF Diamond Mountains, rocks mapped as NCF latitude of Eureka (Fig. 1). More than half deposition to regional deformation, as demon- (Stewart and Carlson, 1978; Kleinhampl and (117 km) of this total shortening was accom- strated by the diverse range of scenarios pro- Ziony, 1985) have been alternatively interpreted modated by emplacement of the Canyon Range posed in previous studies (e.g., Nolan et al., as Permian (Larson and Riva, 1963; Perry and thrust sheet, which may have initiated as early 1974; Vandervoort and Schmitt, 1990; Carpen- Dixon, 1993), with no published biostratigraphic as the latest Jurassic (ca. 145 Ma), and lasted ter et al., 1993; Ransom and Hansen, 1993; age control. The Aptian deposition age defi ned until ca. 110 Ma, when the deformation front Taylor et al., 1993). Based on clast composition in the type exposure (Druschke et al., 2011) migrated forward to the Pavant thrust sheet (Fig. and detrital zircon provenance data indicating provides the only precise age control of any 13) (DeCelles and Coogan, 2006). Therefore, derivation from proximal late Paleozoic sub- NCF exposure to date. Therefore, although it is construction of the Eureka culmination in the crop units, Vandervoort and Schmitt (1990) and possible that other exposures mapped as NCF hinterland was coeval with late-stage emplace- Druschke et al. (2011) suggested that deposition along strike were deposited in a regional belt of ment of the Canyon Range thrust sheet. This in the type-NCF basin may have been contem- Early Cretaceous contractional deformation, the thick, areally extensive thrust sheet is exposed porary with proximal CNTB deformation. How- precise age control and detailed structural con- across all of westernmost Utah and eastern ever, these studies lack the necessary structural text necessary to convincingly demonstrate this Nevada at this latitude, and was translated a total context to relate NCF deposition to motion on are currently lacking, and indicate the need for of 140 km eastward during Sevier orogenesis; specifi c faults or growth of folds. The revised additional mapping and geochronology. this is attributed to high rheological competence CNTB structural model presented here provides as a result of carrying a ~7-km-thick section this context and facilitates interpretation of NCF Implications for Out-Of-Sequence of Neoproterozoic–early Cambrian quartzite deposition from the perspective of the regional Deformation in the Sevier Hinterland (DeCelles, 2004). The dimensions of the Can- preextensional deformation geometry. We pro- yon Range thrust sheet, which approach 250 km pose that the NCF type exposure was deposited The timing of initiation of deformation in the across strike and 700 km along strike (estimate in a piggyback basin that developed on the east- Sevier thrust belt in Utah is a subject of long- includes the correlative Paris-Willard thrust to ern limb of the Eureka culmination as it grew standing debate (e.g., Armstrong, 1968; Jordan, the north; e.g., Armstrong, 1968), rank among (Figs. 12A, 12B). This implies that culmination 1981; Wiltschko and Dorr, 1983; Heller et al., the largest recorded thrust sheets in foreland growth, as well as related motion on the Ratto 1986; DeCelles, 2004). The onset of subsidence thrust belts (Hatcher and Hooper, 1992; Hatcher, Canyon thrust at depth, can be indirectly dated in the Sevier foreland basin, which is attributed 2004), and may approach a critical mechanical as Aptian (ca. 116 Ma; Druschke et al., 2011). to loading from crustal thickening in the Sevier upper bound for this tectonic setting. The total preserved across-strike structural thrust belt, occurred by at least ca. 125 Ma Numerical and analog models predict that the relief of the basal NCF unconformity is ~1.5 km; (Aptian-Barremian boundary) (Jordan, 1981), critical taper angle of an orogenic wedge that structural relief of the eastern limb of the cul- and has been argued to be as old as ca. 145 Ma must be achieved to allow forward propaga- mination approached 4.5 km by the end of its (latest Jurassic) (DeCelles, 2004; DeCelles and tion is governed by the relative magnitudes of construction. This indicates that the NCF was deposited during the early stages of fold growth (Fig. 12B). The most likely sediment source was Active structures in Sevier thrust belt: Pavant thrust Paxton thrust Gunnison erosion of the culmination crest, which is com- Canyon Range thrust and duplex and duplex thrust patible with provenance data suggesting deriva- Eureka culmination tion from proximal late Paleozoic subcrop units (hinterland) Sevier culmination frontal triangle zone (Vandervoort and Schmitt, 1990; Druschke et al., Newark Canyon Formation type-section: Druschke et al. (2010): ~122 Ma youngest 2011) and east-directed paleocurrent directions ? ? DZ peak and ~116 Ma tuff (Aptian) (Vandervoort, 1987). After deposition, the NCF Total shortening in Sevier thrust belt: 221 km 200 211 km continued to be folded during late-stage growth 191 km of the culmination, represented by the northward km 117 km continuation of the Pinto Creek syncline into the 0 100 NCF type exposure (Nolan et al., 1971) (Fig. 140 130 120 110 100 90 80 70 10), which in our structural model corresponds Time (Ma) to the leading axis of the hanging-wall cutoff of the Ratto Canyon thrust sheet (Fig. 12C). Figure 13. Graph showing timing of active structures and cumulative shortening mag- Lateral lithologic variability coupled with nitudes reported for type-Sevier thrust belt (DeCelles and Coogan, 2006). Approximate a lack of precise deposition age control make Aptian deposition age range (125–112 Ma) is shown for Newark Canyon Formation. DZ— regional correlations between isolated NCF detrital zircon.

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the frictional strength of the basal dècolle mont the Eureka culmination, a north-striking anti- Armstrong, R.L., 1968, Sevier orogenic belt in Nevada and Utah: Geological Society of America Bulletin, v. 79, and the compressive strength of the rocks in the cline with a 20 km wavelength, a 4.5 km ampli- p. 429–458, doi:10 .1130 /0016 -7606 (1968)79 [429: orogenic wedge (e.g., Chapple, 1978; Davis tude, and limb dips of 25°–35°, which is cor- SOBINA]2 .0 .CO;2 . et al., 1983; Dahlen et al., 1984; Dahlen, 1990). roborated by deep Paleogene erosion levels that Armstrong, R.L., 1972, Low-angle (denudation) faults, hinterland of the Sevier orogenic belt, eastern Nevada and Assuming that the strength of rocks within the can be traced for ~100 km along strike. A Cam- western Utah: Geological Society of America Bulletin, Canyon Range thrust sheet did not change appre- brian over Silurian relationship observed in drill v. 83, p. 1729–1754, doi: 10 .1130 /0016 -7606 (1972)83 ciably after accretion into the orogenic wedge, a holes under the culmination crest defi nes the [1729: LDFHOT]2 .0 .CO;2 . Armstrong, R.L., and Ward, P., 1991, Evolving geographic decrease in basal frictional strength would be blind Ratto Canyon thrust. The culmination is patterns of Cenozoic magmatism in the North Ameri- necessary for continued eastward translation. interpreted as a fault-bend fold that formed from can Cordillera: The temporal and spatial association of magmatism and metamorphic core complexes: Journal This could be accommodated through several translation of the Ratto Canyon thrust sheet of Geophysical Research, v. 96, p. 13,201–13,224, doi: different mechanisms, including progressive ~9 km eastward over a footwall ramp at depth. 10 .1029 /91JB00412 . strain weakening of fault zone rocks, and/or an The Early Cretaceous (Aptian) type-NCF Bartley, J.M., and Gleason, G.C., 1990, Tertiary normal faults superimposed on Mesozoic thrusts, Quinn increase in pore pressure. An additional mecha- section was deposited in a piggyback basin on Canyon and Grant Ranges, Nye County, Nevada, in nism would be to decrease frictional strength by the eastern limb of the Eureka culmination as it Wernicke , B.P., ed., Basin and Range extensional tec- shortening the length of the basal dècollemont. grew. Aptian hinterland deformation postdated tonics near the latitude of Las Vegas, Nevada: Geologi- cal Society of America Memoir 176, p. 195–212, doi: This was undoubtedly accomplished through migration of the Sevier thrust front into Utah 10 .1130 /MEM176 -p195 . erosional beveling at the thrust front during by ~10–30 m.y., and was coeval with late-stage Barton, M.D., 1987, Lithophile-element mineralization associated with Late Cretaceous two-mica granites translation (e.g., DeCelles, 1994), but could also emplacement of the orogen-scale Canyon Range in the Great Basin: Geology, v. 15, p. 337–340, doi: have been assisted through internal shortening thrust sheet. Growth of the Eureka culmination 10 .1130 /0091 -7613 (1987)15 <337: LMAWLC>2 .0 of the thrust sheet. The ~10 km of hinterland could represent internal shortening of the Can- .CO;2 . Best, M.G., and Christiansen, E.H., 1991, Limited extension shortening at Eureka could represent internal yon Range thrust sheet, which acted as a mecha- during peak Tertiary volcanism, Great Basin of Nevada shortening of the Canyon Range thrust sheet nism to promote further eastward translation. and Utah: Journal of Geophysical Research, v. 96, during emplacement to promote further east- p. 13,509–13,528, doi: 10 .1029 /91JB00244 . ACKNOWLEDGMENTS Best, M.G., Barr, D.L., Christiansen, E.H., Gromme, S., ward translation. Because it was located ~180– Deino, A.L., and Tingey, D.G., 2009, The Great Basin 200 km west of the Canyon Range thrust front This work was funded by grants from the U.S. Altiplano during the middle Cenozoic ignimbrite (preextensional map distance estimated from Geological Survey STATEMAP program and from flareup: Insights from volcanic rocks: International Geology Review, v. 51, p. 589–633, doi:10 .1080 McQuarrie and Wernicke, 2005), construction Timberline Resources Corporation (Paul Dircksen, CEO). The 40Ar/39Ar ages were determined at the /00206810902867690 . of the Eureka culmination may not have appre- Bjerrum, C.J., and Dorsey, R.J., 1995, Tectonic controls New Mexico Geochronology Research Laboratory on deposition of Middle Jurassic strata in a retroarc ciably increased the overall surface slope angle (New Mexico Institute of Mining and Technology) foreland basin, Utah-Idaho trough, western interior, of the orogenic wedge. However, instead of under the guidance of Bill McIntosh, Matt Heizler, United States: Tectonics, v. 14, p. 962–978, doi: 10 building taper, perhaps this hinterland deforma- and Lisa Peters. U-Pb zircon data were acquired at .1029 /95TC01448 . the (U-Th)/He Geo- and Thermochronometry Lab at Boyer, S.E., and Elliott, D., 1982, Thrust systems: American tion acted as a mechanism to decrease the over- the University of Texas at Austin with guidance from Association of Petroleum Geologists Bulletin, v. 66, all frictional coupling of the basal dècollemont Daniel Stockli. We thank Jennifer Mauldin and Irene p. 1196–1230. to promote forward propagation. Seelye of the Nevada Bureau of Mines and Geology Brew, D.A., 1961a, Lithologic character of the Diamond Peak Formation (Mississippian) at the type locality, Eureka Studies focused on the kinematic develop- cartography team, and Mitch Casteel, Bob Thomas, and White Pine Counties, Nevada: U.S. Geological Sur- ment of the frontal Sevier thrust belt in Utah Peter Rugowski, Russell DiFiori, and Lucia Patter- vey Professional Paper 424-C, p. C110–C112. son of the Timberline Resources Corporation Eureka Brew, D.A., 1961b, Relation of Chainman Shale to Bold Bluff have revealed the importance of out-of-sequence exploration team. Comments from three anonymous thrust fault, southern Diamond Mountains, Eureka and growth of structural culminations in the internal reviewers and associate editor Terry Pavlis signifi - White Pine Counties, Nevada: U.S. Geological Survey parts of the thrust belt as a mechanism to drive cantly improved this manuscript. Professional Paper 424-C, p. C113–C115. 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