long an upper-crustal fold province in the hinterland of the sevier … · 2019. 12. 3. · long...

Long

404 Geosphere, April 2015

An upper-crustal fold province in the hinterland of the Sevier orogenic belt, eastern Nevada, U.S.A.: A Cordilleran

Valley and Ridge in the Basin and Range

Sean P. Long1,*1Nevada Bureau of Mines and Geology, University of Nevada, Reno, Nevada 89557, USA

ABSTRACT

Overprinting Cenozoic extension hinders analysis of Cordilleran contractional defor-mation in the hinterland of the Sevier thrust belt in Nevada. In this study, a 1:250,000 scale paleogeologic map of eastern Nevada, showing spatial distributions of Paleozoic–Mesozoic rocks beneath a Paleogene uncon-formity, is combined with dip magnitude maps for Paleozoic–Mesozoic and Tertiary rocks, published sedimentary thickness records, and a published reconstruction of extension, in order to defi ne and regionally correlate thrust faults and folds, and estimate the pre-extensional amplitude, wavelength, and limb dips of folds. A new structural prov-ince, the Eastern Nevada fold belt, is defi ned, consisting of a 100-km-wide region contain-ing fi ve fi rst-order folds that can be traced for map distances between 100 and 250 km and have amplitudes of 2–4 km, wavelengths of 20–40 km, pre-extensional limb dips typi-cally between 10° and 30°, and deform rocks as young as Jurassic and Early Cretaceous. No regional-scale thrust faults or décolle-ment horizons breach modern exposure levels in the Eastern Nevada fold belt. First-order folds of the Eastern Nevada fold belt are interpreted to have formed above a deep (≥10 km below the Paleogene unconformity), blind décollement or shear zone, perhaps the westward projection of the master décolle-ment of the Sevier thrust belt.

Three hinterland structural provinces, the Central Nevada thrust belt, Western Utah thrust belt, and the intervening Eastern Nevada fold belt, collectively record low-mag-nitude (a few tens of kilometers), upper-crustal shortening that accompanied Cretaceous translation of the Cordilleran passive-margin

basin ~220 km eastward during the Sevier orogeny. Low deformation magnitudes in the hinterland are attributed to the rheological competence of this thick basin.

INTRODUCTION

The Jurassic–Paleogene Cordilleran oro-genic belt is the result of over 100 m.y. of con-tractional deformation of the North American plate above an Andean-style subduction zone (Allmendinger, 1992; Burchfi el et al., 1992; DeCelles, 2004; Dickinson, 2004). In the west-ern interior United States, the majority of Cor-dilleran crustal shortening was accommodated in the Sevier thrust belt in western Utah (Fig. 1; e.g., Armstrong, 1968; Royse et al., 1975; Vil-lien and Kligfi eld, 1986; DeCelles and Coogan, 2006). Decades of study in the Sevier thrust belt leave the geometry, kinematics, magnitude, and timing of deformation well documented (e.g., Jordan, 1981; Allmendinger et al., 1983, 1987; Royse, 1993a; DeCelles et al., 1995; Mitra, 1997; DeCelles and Coogan, 2006). However, in the hinterland of the thrust belt in eastern Nevada, fundamental questions remain regarding the style, geometry, and magnitude of Cor dilleran deformation, and how it relates tem porally to deformation in the frontal thrust belt (e.g., Arm-strong, 1972; Miller et al., 1988; Miller and Hoisch, 1995; Camilleri and Chamberlain, 1997; Taylor et al., 2000; Long, 2012; Greene, 2014; Long et al., 2014). This can be attributed in part to sparse preservation of synorogenic sedimen-tary rocks, but it is primarily due to the com-plex dismemberment of the region by Cenozoic extension (e.g., Gans and Miller, 1983; Coney and Harms, 1984; Dickinson, 2002).

Two zones of thrust faults, the Central Nevada thrust belt and Western Utah thrust belt (Fig. 1), have been identifi ed in the Sevier hinter land, and they are interpreted as contem-porary, interior components of the Sevier thrust

system (Taylor et al., 2000; Long, 2012; Greene, 2014; Long et al., 2014). The region of eastern Nevada between the Central Nevada thrust belt and Western Utah thrust belt is interpreted to have experienced relatively little upper-crustal Cordilleran contractional deformation (e.g., Armstrong, 1972; Speed et al., 1988). This is primarily based on compilation maps of strati-graphic levels exposed beneath a regional unconformity that places Paleogene rocks over Paleozoic–Mesozoic rocks, which show that the total postorogenic structural relief of this region was low (2–4 km; Armstrong, 1972; Gans and Miller, 1983; Long, 2012). In addition, early mapping studies in eastern Nevada documented that angularity across the unconformity is typi-cally ≤10°–15° (Young, 1960; Kellogg, 1964; Moores et al., 1968), which has led to a prevail-ing view that any pre-Tertiary deformation was gentle and minor.

However, despite the low structural relief of this region, the map patterns of regionally trace-able (≥100 km) folds are defi ned on subcrop maps (Gans and Miller, 1983; Long, 2012), and detailed geologic maps (Humphrey, 1960; Bro-kaw and Barosh, 1968; Nolan et al., 1971; Nutt, 2000) show that many more folds are present, although to date they have not been regionally correlated or described in detail. Recent work near Eureka that documents 60°–70° of angu-larity across the Paleogene unconformity (Long et al., 2014), and geologic maps showing fold limb dips ranging from 30° to overturned (Hum-phrey, 1960; Larson and Riva, 1963; Brokaw and Barosh, 1968; Nolan et al., 1971) both chal-lenge the interpretation of minimal pre-Tertiary deformation and justify a structural synthesis of this region.

In this study, the primary goal is to describe folding in the region between the Central Nevada thrust belt and Western Utah thrust belt; this exercise leads to defi nition of a new struc-tural province, the Eastern Nevada fold belt.

Geosphere; April 2015; v. 11; no. 2; p. 404–424; doi:10.1130/GES01102.1; 7 fi gures; 2 tables; 1 plate; 2 supplemental fi les.Received 11 July 2014 ♦ Revision received 2 December 2014 ♦ Accepted 16 January 2015 ♦ Published online 17 February 2015

*E-mail: [email protected].

For permission to copy, contact [email protected]© 2015 Geological Society of America

A fold province in the Sevier hinterland in eastern Nevada

Geosphere, April 2015 405

A 1:250,000 scale paleogeologic map of east-central Nevada, constructed by compiling for-mation-scale divisions of Paleozoic–Mesozoic rocks exposed beneath the Paleogene unconfor-mity, is presented. Subcrop patterns defi ned on the map allow regional correlation of fold axes,

and these are combined with published sedi-mentary thicknesses (Stewart, 1980) to estimate fold amplitude. The map is combined with dip magnitude maps for Paleozoic–Mesozoic and Tertiary rocks, which corroborate the correlation of fold axes and allow estimation of pre-Paleo-

gene limb dips. Fold axes are superimposed over a pre-extensional tectonic reconstruction (McQuarrie and Wernicke, 2005), which illus-trates the synorogenic map dimensions of indi-vidual structures and structural provinces and allows estimation of fold wavelength.

ESTB

Sierra Nevad

a mag

matic arc

GC-RR-ARMT

GTR-EH

CN

TB

SR

LFTB

Great Valley forearc b

asin

Franciscan

accretionary

complex

ESTB

Sierra Nevad

a mag

matic arc

RMTGT

Se

vie

r fo

ld-

thru

st b

elt

CN

TB

LFTB

Great Valley fo

rearc basin

Franciscan

accretion

ary com

plex

WU

TB

?

WU

TB

EN

FB

Sevi

er fo

ld-

thru

st b

elt

EN

FB

N

N

NVCA

UT

WY

AZ

OR ID

NVCA

UT

WY

AZ

ORID

0 200100

kilometers

0 200100

kilometers

area of

Figure 5

area of

Figure 6

area of

Plate 1

36 Ma

Present dayLas

Vegas

Salt

Lake

City

EurekaRenoAustin

Ely

Elko

Tonopah

Cedar

City

37°N

41°N

39°N

111°W114°W117°W120°WA

B

Figure 1. (A) Map of the Cordi-lleran retroarc region in Nevada, Utah, and eastern California, superimposed over a base map from McQuarrie and Wernicke (2005, their Fig. 7A), which shows present-day dimensions. Defor-mation fronts of Cordilleran thrust systems are shown, and spatial extents are shaded gray; locations are modifi ed from Long et al. (2014), with additions from Greene (2014) and this study. Area of Eastern Nevada fold belt (ENFB) is shaded blue. Paleozoic–early Mesozoic thrust systems are shown in brown. Location of Sierra Nevada magmatic arc is from Van Buer et al. (2009) and DeCelles (2004). (B) Map of same area as A, but superimposed over a base map from McQuarrie and Wer-nicke (2005, their Fig. 9E) which shows a 36 Ma tectonic recon-struction. The map shows approx-imate pre-extensional dimensions of the Cordilleran retroarc region. Abbreviations: GT—Golconda thrust, RMT—Roberts Moun-tains thrust, LFTB—Luning-Fencemaker thrust belt; ESTB—Eastern Sierra thrust belt; CNTB—Central Nevada thrust belt; ENFB—Eastern Nevada fold belt; WUTB—Western Utah thrust belt; R-EH—Ruby–East Humboldt core complex; SR—Snake Range core complex; GC-RR-A—Grouse Creek–Raft River–Albion core complex. State abbreviations: CA—California, OR—Oregon, NV—Nevada, ID—Idaho, UT—Utah, WY—Wyo-ming, AZ—Arizona.

Long


In addition, the subcrop map provides a detailed view of the map patterns of thrust faults and folds in the northern Central Nevada thrust belt, including the recently defi ned Eureka cul-mination (Long et al., 2014). These observa-tions are combined with the structural synthesis of the Eastern Nevada fold belt and published cross sections of the Western Utah thrust belt (Greene, 2014) and Sevier thrust belt (DeCelles and Coogan, 2006) to present a model for con-tractional deformation in the Sevier hinterland.

TECTONIC SETTING

The Sevier thrust belt represents part of the Cordilleran retroarc thrust belt system, which extends from Mexico to Alaska, and formed during Jurassic to Paleogene contractional deformation of the North American plate above subducting oceanic plates (e.g., Allmendinger, 1992; DeCelles, 2004; Dickinson, 2004). The Cordilleran magmatic arc at the latitude of Nevada is represented by the Sierra Nevada batholith (Fig. 1; e.g., Coleman and Glazner, 1998; Ducea, 2001). East of the magmatic arc, the Luning-Fencemaker thrust belt (Fig. 1) is interpreted to record Jurassic closure of a back-arc basin (e.g., Oldow, 1984; Wyld, 2002). The genetic relationship between the Luning-Fence-maker and Sevier thrust belts is debated; Wyld (2002) argued that these two systems represent deformation during distinct Jurassic and Creta-ceous tectonic events, while DeCelles (2004) interpreted the Luning-Fencemaker thrust belt as an older, hinterland component of the Sevier orogenic wedge.

To the east of the Luning-Fencemaker thrust belt, there lie two zones affected by Paleozoic to early Mesozoic orogenic events. The oldest is the Mississippian Antler orogeny, in which Ordovi-cian to Devonian, deep marine, sedimentary and volcanic rocks were emplaced eastward over shelf rocks across the Roberts Mountains thrust and related structures (Fig. 1; e.g., Burchfi el and Royden, 1991; Speed and Sleep, 1982; Dick-inson, 2000), and the youngest is the Triassic Sonoma orogeny, where Devonian to Permian , deep marine, sedimentary and vol canic rocks were translated eastward over the Golconda thrust (Fig. 1; e.g., Oldow, 1984; Miller et al., 1992; Dickinson, 2000).

Farther to the east, the Central Nevada thrust belt and Western Utah thrust belt (Fig. 1) are zones of north-striking, dominantly east-ver-gent thrust faults and folds that branch off of the Sevier thrust belt, and each accommodated ~10 km of shortening (Bartley and Gleason, 1990; Taylor et al., 1993, 2000; Long, 2012; Greene, 2014; Long et al., 2014). Though defor-mation timing constraints are broad, the Cen-

tral Nevada thrust belt and Western Utah thrust belt are interpreted to represent contemporary, interior components of the Sevier thrust system (Taylor et al., 2000; Greene, 2014; Long et al., 2014). The region of eastern Nevada between these two thrust belts, which is the subject of this paper, exhibits upper-crustal folding but lacks regional-scale thrust faults (e.g., Arm-strong, 1972; Gans and Miller, 1983). However, this region did experience Cordilleran ductile deformation and metamorphism at midcrustal levels, as recorded by Late Cretaceous peak metamorphism and ductile fabrics in rocks now exposed in metamorphic core complexes and highly extended ranges (e.g., Miller et al., 1988; Miller and Gans, 1989; McGrew et al., 2000; Wells and Hoisch, 2008).

On the east end of the Cordilleran defor-mation system, the Sevier thrust belt accom-modated ~220 km of upper-crustal shortening in western Utah (Currie, 2002; DeCelles and Coogan, 2006). The timing of initial deforma-tion in the Sevier thrust belt is debated (e.g., Jordan, 1981; Wiltschko and Dorr, 1983; Heller et al., 1986; DeCelles, 2004; DeCelles and Coogan, 2006), but most agree that the onset of subsidence in the adjacent foreland basin, which is attributed to crustal thickening in the Sevier thrust belt, occurred by at least ca. 125 Ma (Early Cretaceous; Jordan, 1981). However, initial motion on the westernmost fault of the thrust belt has been argued to be as old as ca. 145 Ma (Jurassic-Cretaceous boundary; DeCelles, 2004; DeCelles and Coogan, 2006). Deforma-tion in the Sevier thrust belt at this latitude con-tinued through the Late Cretaceous and Paleo-cene (Lawton and Trexler, 1991; Lawton et al., 1993, 1997; DeCelles et al., 1995; DeCelles and Coogan, 2006), on the basis of geochronology, biostratigraphy, and structural relationships of foreland basin strata.

The hinterland of the Sevier thrust belt in western Utah and eastern Nevada is the hypoth-esized site of a relict orogenic plateau (e.g., Coney and Harms, 1984; Allmendinger, 1992; Jones et al., 1998; Dilek and Moores, 1999; DeCelles, 2004; Best et al., 2009). The existence of this plateau, termed the “Nevadaplano” after comparison to the modern Andean Altiplano-Puna (Allmendinger, 1992; Jones et al., 1998; DeCelles, 2004), is supported by restoration of Tertiary extension (Coney and Harms, 1984) and estimation of crustal shortening accom-modated in the Sevier thrust belt (DeCelles and Coogan, 2006), which both suggest that crustal thicknesses of at least 50 km were achieved in the hinterland region by the end of shortening. These crustal thicknesses may have supported surface elevations as high as 3 km (DeCelles and Coogan, 2006; Snell et al., 2014).

METHODS

Paleogeologic Map

Plate 1 presents a paleogeologic map of east-central Nevada that shows the distribution of Paleozoic and Mesozoic sedimentary rocks exposed under a regional unconformity beneath Paleogene volcanic and sedimentary rocks (see Fig. 2 for a guide to range, valley, and other geographic names). This form of map removes the vertical effects of tectonism that postdate the unconformity (e.g., Armstrong, 1968), including differential uplift and subsidence associated with Neogene normal faulting. When combined with stratigraphic thickness data (Stewart, 1980) and structural data from published geologic maps, this map can be used to illustrate the map pat-terns of pre-Paleogene structures, and to estimate Paleogene structural relief, the amplitude of ero-sionally beveled folds, and stratigraphic throw on thrust faults at Paleogene erosion levels.

The map was constructed by fi rst georefer-encing 50 published geologic maps, the majority of which are between 1:24,000 and 1:62,500 in scale, and four 1:250,000 scale Nevada county geologic maps (see Plate 1 for guide to source maps). Then, following methods outlined in Long (2012), all locations of exposures of the Paleogene unconformity were compiled, and the ages of Paleozoic–Mesozoic sedimentary rocks that directly underlie the unconformity at each locality were divided out (where possible) at the formation scale. Across the majority of the map area, the oldest preserved Paleogene rocks are late Eocene to Oligocene volcanic rocks of the Great Basin ignimbrite fl are-up (e.g., Armstrong and Ward, 1991; Best and Christiansen, 1991; Best et al., 2009). Less commonly, alluvial and lacustrine rocks of the Sheep Pass Forma-tion, which have been interpreted to represent deposition within isolated extensional basins (Druschke et al., 2009a), are preserved beneath ignimbrite fl are-up rocks. Within the map area, the Sheep Pass Formation is interpreted as Paleocene to Eocene in age (Hose and Blake, 1976; Kleinhampl and Ziony, 1985; Lund et al., 1988; Vandervoort and Schmitt, 1990; Fouch et al., 1991), although farther east in Nevada, it has been interpreted to be as old as Maas-trichtian (Druschke et al., 2009b). Localities where late Eocene to Oligocene volcanic rocks versus Paleocene to Eocene sedimentary rocks overlie the unconformity are not differentiated on Plate 1, and therefore the total age range of unconformities compiled spans the Paleogene.

In total, 1024 individual locations of surface exposures of the Paleogene unconformity were compiled. In addition, in 809 places where the unconformity was not exposed, the age of the



40

°00

’N3

9°3

0’N

39

°00

’N3

8°3

0’N

38

°00

’N

116°15’W 115°00’W115°30’W116°00’W

40

°00

’N3

9°3

0’N

39

°00

’N3

8°3

0’N

38

°00

’N

115°00’W115°30’W116°00’W

1 - Roberts et al. (1967)

2 - Hose and Blake (1976)

3 - Kleinhampl and Ziony (1985)

4 - Tschanz and Pampeyan (1970)

5 - Carlisle and Nelson (1990)

6 - Haworth (1979)

7 - Colgan et al. (2010)

8 - Millikan (1979)

9 - McKee and Conrad (1998)

10 - Lipka (1987)

11 - Larson and Riva (1963)

12 - Nutt and Hart (2004)

13 - Nutt (2000)

14 - Connell (1985)

15 - Otto (2008)

16 - Fritz (1968)

17 - Low (1982)

18 - Bentz (1983)

19 - Drake (1978)

20 - Nolan et al. (1971)

21 - Nolan (1962)

22 - Campbell (1981)

23 - Tomastik (1981)

24 - Douglass (1960)

25 - Schalla (1978)

26 - Simonds (1997)

27 - Long et al. (2012)

1

2

3

4

5 6

78

9

1011

12

13

14

15

16

17

18

19

20

21

22

23

24

2526

27

28 29

30

31

32

33

34

35

36

37

3839

40 41 42

43

45 4647

48

49

50

51

52

5354

C Geologic map sources

Plate 1

44

28 - Cowell (1986)

29 - Nolan et al. (1974)

30 - Humphrey (1960)

31 - Feeley (1993)

32 - Brokaw and Barosh (1968)

33 - Hose (1983)

34 - McDonald (1989)

35 - Guerrero (1983)

36 - Tracy (1969)

37 - Brokaw and Heidrick (1966)

38 - Dixon et al. (1972)

39 - Moores et al. (1968)

40 - Ekren et al. (1973A)

41 - Quinlivan et al. (1974)

42 - Lund et al. (1987)

43 - Lund et al. (1988)

44 - Camilleri (2013)

45 - Snyder et al. (1972)

46 - Ekren et al. (1972)

47 - Fryxell (1988)

48 - Ekren et al. (1973B)

49 - Martin and Naumann (1995)

50 - Ekren et al. (2012)

51 - Bartley and Gleason (1990)

52 - Bartley and Gleason (1990)

53 - Overtoom (1994)

54 - duBray and Hurtubise (1994)

Source maps:

0 5 10 15 20 25Scale: 1:250,000

kilometers

D Map explanation

B Paleogene subcrop map of east-central Nevada

Y

Subcrop data:

E

Subcrop beneath exposure of Paleogene unconformity

Youngest possible subcrop beneath Paleogene unconformity

Youngest possible subcrop beneath Paleogene unconformity

in drill hole

Subcrop beneath Paleogene unconformity in drill hole

Easternmost exposure of rocks in hanging wall of Roberts

Mountains thrust

Y

anticline axis at Paleogene erosion surface

Map symbols:

syncline axis at Paleogene erosion surface

thrust fault (teeth on upthrown side)

pre-unconformity normal fault (ball on

downthrown side)

post-unconformity normal fault (ball on

downthrown side)

stratigraphic contact between subcrop units

road

203

199

36 strike and dip of rocks during Paleogene; brown

number corresponds to Figure SM1

horizontal rocks during Paleogene; brown

number corresponds to Figure SM1

county boundary

No data: extensive

volcanic coverN

Structure abbreviations:Sulphur Springs Range and southern Fish Creek Range:

RMT - Roberts Mountains thrust

Antelope Range and Park Range:

AT - Antelope thrust

Fish Creek Range and Diamond Mountains:

EC - Eureka culmination

WMA - White Mountain anticline

DTF - Dugout Tunnel fault

HFS - Hoosac fault system

PSF - Pinto Summit fault

SMS - Sentinel Mountain syncline

MNT - Moritz-Nager thrust

Northern Pancake Range:

MPT - Moody Peak thrust

PTS - Pancake thrust system

SRS - Silverado Ridge syncline

GST - Green Springs thrust

DT - Duckwater thrust

Railroad Valley and southern Pancake Range:

PMT - Portuguese Mountain thrust

MSS - McClure Spring syncline

TSA - Trap Spring anticline

BFS - Bacon Flat syncline

White Pine Range and Bald Mountain:

ST - Shellback thrust

LAS - Little Antelope syncline

Grant Range and Quinn Canyon Range:

TMA - Timber Mountain anticline

SCT - Schofield Canyon thrust

RT - Rimrock thrust

SMT - Sawmill thrust

RMT

Pinto

Creek

syncline

EC

EC

Butte

synclinorium

TMA

RT

RMT

AT

SMT

Illipah

anticline

LAS

MSS

BFSTSA

MPT

PTS

SRS

PTS

GST

PMT

DT

WMA

DTF

HFS

PSF

MNTSMS

ST

SCT

thrust fault structurally below Paleogene erosion

surface (teeth on upthrown side)

Cherry

Creek

anticline

Geographic coordinate system: NAD 1983

anticline axis structurally below Paleogene erosion

surface

axis of 1st-order Eastern Nevada fold belt anticline

at Paleogene erosion surface

axis of 1st-order Eastern Nevada fold belt syncline

at Paleogene erosion surface

Illipah

anticline

Butte

synclinorium

Pinto

Creek

syncline

14

43

22

37

51 12

19

31

1414

66

63

61

69

53

23

1817

26

33

15

26 49

12

36

9

30

221210

8

26

29

6

15

18

26

36

7

11

17

13

5810 11

19

4

4

11

3

31

8

11

14

30

9

40

24

6

21

26

12

13

33

39

9

45

28

1357

5

22

23

24

25

26

27

28

30 32

52

53

54

55 56

57

58

59

60

66

73

76

79

98

100

101102

106

108

111

115

118

121

135

137

139

141

145

147149

151

154 156

160

162

168

171

180

183

185

188

190

192

194

197 199

203

208

213

216

218

223

225

227

229 231

240

245

247

249

251

253

Tertiary

Cretaceous

Jurassic

Triassic

Me

sozo

icC

en

ozo

icPaleocene

Eocene

Lower

intrusive rocks:

Permian

Pennsylvanian

Lower

Lower

Upper

Moenkopi Formation

and Thaynes Formation

megabreccia (landslide blocks)

Park City Group

Garden Valley

Formation

Carbon Ridge

Formation

Rib Hill

Sandstone

Arcturus

Formation

Arcturus Fm.

and Rib Hill

Sandstone,

undiff.

Permian,

undiff.

Pennsylvanian-Permian, undiff.

Newark Canyon Formation

Upper

Footnotes for correlation chart:1. Megabreccia units Klnc, Klcr, Kle, and Kln from Nolan et al. (1971) are mapped as KTmbr in the southern Diamond Mountains. In the Roberts Mountains, slide blocks of

Ddg lying over Ov are mapped as KTmbr (McKee and Conrad, 1998).

2. Permian Unit G (Pgl, Pgu) from Larson and Riva (1963) mapped as Knc, after Stewart (1980), Stewart and Carlson (1978), and Haworth (1979).

3. Includes the Kaibab limestone, Gerster Formation (Douglass, 1960), and Plympton Formation (Connell, 1985), after Hose and Blake (1976).

4. Includes the Loray and Pequop formations (Connell, 1984), after Hose and Blake (1976).

5. Lies unconformably on either Mississippian rocks or Ordovician Vinini Formation (McKee and Conrad, 1998; Carlisle and Nelson, 1990)

6. Units Pa through Pf of Larson and Riva (1963) are mapped as Pcr after Hose and Blake (1976) and Roberts et al. (1967).

7. Includes Reipe Spring Limestone in Egan Range (Brokaw and Heidrick, 1966) and Pancake Range (Kleinhampl and Ziony, 1985).

8. Interpreted in drill holes in Railroad Valley, White River Valley, Long Valley, and White Pine Range (Hess et al., 2004).

9. Pennsylvanian Moleen Limestone and Tomera Formation of Campbell (1981) and Tomastik (1981) are mapped as IPe here.

10. Mdp is typically only divided out in source maps in the northwest quarter of the map area.

11. Includes unit Ms locally divided out by Kleinhampl and Ziony (1985), and unit Msw (Scotty Wash sandstone) of duBray and Hurtubise (1994).

12. Only in the southwest part of the map area. Ekren et al. (1973A) maps Me above Dn; Ddg was either not deposited here, or was eroded prior to Me deposition.

13. Units Mar and Marc of Hose (1983) are mapped as Mdc here, after stratigraphic divisions of Nolan et al. (1974). Mdc is local to Fish Creek and Diamond ranges. Also, in

the Mahogany Hills, unit ‘u’ of Schalla (1978) (undifferentiated post-Devonian sandstone, shale, and conglomerate) is mapped here as Mdc, after Long et al. (2012).

14. Lower Mississippian Webb Formation (Mw) of Hose (1983) is mapped here as Joana Limestone.

15. Only mapped in Fish Creek Range; allochthonous Dw of Hose (1983) is interpreted as upper plate of Roberts Mountains allochthon, after Stewart and Carlson (1978).

16. Named Devil’s Gate Limestone within and west of the Diamond Mountains, and Guilmette Formation to east and south; these two units are laterally-equivalent.

17. Includes Bay State Dolomite, Woodpecker Limestone, and Sentinel Mountain Dolomite members in the Diamond Mountains (Nolan et al., 1974), and Simonson

Dolomite member elsewhere.

18. Includes Oxyoke Canyon Sandstone and Beacon Peak Dolomite members in Diamond Mountains (Nolan et al., 1974), and Oxyoke Canyon Sandstone member, Sadler

Ranch Fm., McColley Canyon Fm., and Beacon Peak Dolomite member in Fish Creek Range (Hose, 1983; Cowell, 1986; Long et al., 2012). Consists of Sevy Dolomite in

the majority of the map area, including Quinn Canyon Range and Railroad Valley (Ekren et al., 2012; Hess et al., 2004).

19. Includes the laterally-equivalent Laketown Dolomite mapped by Kleinhampl and Ziony (1985) and Ekren et al. (2012).

20. Includes Ely Springs Dolomite in Pancake and Quinn Canyon ranges (Kleinhampl and Ziony, 1985; Ekren et al., 2012); laterally-equivalent to Hanson Creek Dolomite.

21. Includes the Antelope Valley, Ninemile, and Goodwin Formations in the Fish Creek and Antelope Ranges (Hose, 1983; Long et al., 2012). Also includes the Copenhagen

Formation of Hose (1983) in the southern Antelope Range.

22. Both Cdw and Chs are only exposed in the Fish Creek Range (Nolan et al., 1974; Long et al., 2012).

Abbreviations used in correlation chart: undiff. = undifferentiated; Fm. = Formation; Sh. = shale; Ls. = limestone

1

2

8

3

4

75 6

LowerEly Limestone9

Mississippian

Diamond Peak

FormationUpper

Chainman

Shale

10

11Diamond Pk. Fm.

and Chainman

Shale, undiff.

Lower 13Dale Canyon Fm.

UpperJoana Limestone and

Pilot Shale, undiff.Diamond Peak Fm.,

Chainman Sh., Joana Ls.,

and Pilot Sh., undiff.

Chainman Sh.,

Joana Ls., and

Pilot Sh. undiff.

Eleana Fm.

Devonian

12

14

Middle

Devil’s Gate limestone

and Guilmette Fm.

Woodruff Fm.15

16

Upper Nevada Fm.

Lower Nevada Fm.Lower Nevada Fm., undiff.

17

18

SilurianLone Mountain Dolomite19

OrdovicianEureka Quartzite and

Hanson Creek Formation

Upper

Middle

Lower

Vinini Fm.20

Pogonip Group,

undiff.21

Cambrian

Windfall Formation and

Dunderberg Shale, undiff.22

22

Upper

Middle Hamburg dolomite and

Secret Canyon Shale, undiff.

Pa

leo

zoic

Oligocene sub-volcanic

unconformity

basal Sheep Pass

Fm. unconformity

late Eocene

allochthonous

rocks in hanging

wall of Roberts

Mountains thrust:

Ki

Ji

Dw

Ov

Ddg

Dnu

Dnl

Dn

Slm

Oe

Op

Cdw

Chs

IPPuPrhPcrPgv

IPe

Mdp

Mc

Mcd

Mdc

MDpj

MDpjcd

MDpjcMe

KTmbr

Knc

TRmt

Pu

Ppc

Pa

Par

A Correlation of map units

Ru

by M

ou

ntain

s

Hu

ntin

gto

n V

alley

Tab

le M

tn.

Pin

e V

alle

y

Gar

de

n V

alle

y

Ro

be

rts

Mts

.

Su

lph

ur

Sp

rin

gs

Ran

ge

Dia

mo

nd

Va

lley

Kobeh Valley

Wh

istler Mtn

.

Lon

e M

tn.

Mtn. Boy Range

Ma

ho

ga

ny

Hill

s

An

telo

pe

Va

lley

Fish

Cre

ek

Ran

ge

Eureka

Dia

mo

nd

Mts.

Litt

le S

mo

ky V

alle

y

Pan

cake

R.

Ne

wark V

alley

Diam

on

d M

ts.

Ru

by V

alley

Bald

Mo

un

tain

Maveric

k Spr.

R.

Bu

tte

Mo

un

tain

s

Bu

tte

Val

ley

Ch

err

y C

ree

k R

ang

e

Lon

g V

alle

y

Bu

ck M

ou

nta

in

Ne

wark V

alley

Strawberry

Eg

an R

ang

e

Rad

ar Rid

geJa

ke’s Va

lley

Wh

ite P

ine

Ra

ng

e

Hamilton

Wh

ite P

ine

Ra

ng

e Preston

Lund

Currant

Eg

an R

ang

e

Wh

ite

Riv

er V

alle

y

Sunnyside

Eg

an R

ang

e

Seaman Range

Co

al Valle

y

Go

lde

n G

ate

Ran

ge

Gar

den

Val

ley

Gra

nt

Ran

ge

Qui

nn

Can

yon

Ran

ge

Rai

lro

ad V

alle

y

Re

veill

e R

an

ge

Pan

cake

Ran

ge

Lockes

Ho

t C

ree

k V

alle

y

Rai

lro

ad V

alle

y

Big

Sand

Sp

ring

s Va

lley

Ho

t C

ree

k R

ang

e

Par

k R

ang

e

Ra

ilro

ad

Va

lley

Duckwater

Du

ckw

ate

r H

illsPancake Range

Little Smo

ky Valley

An

telo

pe

R.

Plate 1. Paleogene subcrop map of east-central Nevada at 1:250,000 scale, with a correlation chart of map units, an index to geologic map sources, and an explanation of subcrop data, map symbology, and structure abbreviations. Strike and dip symbols show attitudes of rocks during the Paleogene, after retrodeformation of tilts of Tertiary rocks; brown numbers next to strike and dip symbols correspond to stereoplots in Figure SM1 in the supplemental fi le (see text footnote 1). For a full-sized PDF fi le of Plate 1, please visit http:// dx .doi .org /10 .1130 /GES01102 .S1 or the full-text article on www .gsapubs .org.

Long


youngest pre-unconformity stratigraphic unit was compiled (data marked with a “Y” on Plate 1), which constrains the lowest possible stratigraphic level of the unconformity. Finally, formation top logs from 116 drill holes (Hess et al., 2004) were also used to locate the exact (n = 77) or lowest possible stratigraphic level (n = 39) of the Paleogene unconformity. All sup-porting subcrop and drill-hole data are shown on Plate 1, and accompanying ArcGIS data fi les and a pdf of the paleogeologic map that contains layers that can be turned on and off are included in the Supplemental File.1

Structural and stratigraphic contacts on Plate 1 were determined from interpretations and geometries shown in source mapping, and their locations were determined by interpolation between subcrop data points. The spatial density of subcrop data points is highly variable and is a function of multiple factors, including density of bedrock exposure and the degree of preserva-tion of rocks above the Paleogene unconformity. Therefore, except in the places where structural and stratigraphic contacts are precisely located between closely spaced data points, contacts should be interpreted as approximately located. Fold axes shown on Plate 1 were precisely located off of source mapping, where possible, and are based on interpolation of subcrop data points elsewhere. The formation-scale resolu-tion of subcrop data, as well as incorporation of structural data from detailed source maps, allowed mapping of faults and fold axes in many areas where the lower-resolution subcrop map of Long (2012) could not.

Plate 1 differs from a standard geologic map in several ways, and therefore several assump-tions must be defi ned for interpretation of this map: (1) It is assumed that all rocks are assigned to the correct geologic formation on source maps, and that interpretations of strati-graphic and structural contacts on source maps are correct; (2) using stratigraphic thicknesses

40

°00

’N3

9°3

0’N

39

°00

’N3

8°3

0’N

38

°00

’N

115°00’W115°30’W

Ru

by M

ts.

Hu

ntin

gto

n V

alley

Tab

le M

tn.

Gar

de

n V

ly.

Ro

be

rts

Mts

.

Sulp

hu

r Sp

rin

gs

R.

Dia

mo

nd

Va

lley

Ko

beh

Vly.

Wh

istler Mtn

.

Devil’s

Gate

Lon

e M

tn.

Mtn. Boy R.

Mah

og

any

Hill

s

An

telo

pe

Vly

.Eureka

Prospect

Peak

Diamond

Peak

Fish

Ck.

Ran

ge

Litt

le S

mo

kyV

alle

y

Pan

cake

Ran

ge

Pancake

SummitD

iam

on

d M

ou

nta

ins

Ru

by V

ly.

Bald

Mo

un

tain

Mav

eric

k Sp

rings

R.

Ch

err

y C

ree

k R

ang

e

Lon

g V

alle

y

Bu

ck M

ou

nta

in

New

ark Valley

Strawberry

Bu

tte

Mo

un

tain

s Bu

tte V

alley

Big

Bald

Mtn.

Eg

an

Ra

ng

e

Rad

ar Rid

ge

Jake’s V

alle

y

Wh

ite P

ine

Ra

ng

e

Hamilton

Mt. Hamilton

Currant

Mtn.Preston

Lund

Currant

Eg

an

Ra

ng

e

Ho

rse R

ang

e

Wh

ite

Riv

er

Val

ley

Sunnyside

Eg

an R

ang

e

White River Valley

Seaman Range

Co

al Valle

y

Go

lden

Gat

e R

ang

e

Gar

den

Val

ley

Troy Peak

Gra

nt

Ran

ge

Quin

n Can

yon R

ange

Rai

lro

ad V

alle

yRe

veille

Ra

ng

e

Pan

cake

Ran

ge

Lockes

Portuguese

Mtn.

Lunar

Crater

Ho

t C

ree

k V

alle

y

Rai

lro

ad V

alle

y

Big

San

d S

pri

ng

s Va

lley

Ho

t C

ree

k R

ang

eP

ark

Ran

ge

Duckwater

Du

ckw

ate

r H

ills

Pancake R

ang

e

Moody PeakAn

telo

pe

Ra

ng

e

U.S. Hwy. 50

U.S

. Hw

y. 6

Nye County

White Pine County

Eureka County

Lincoln County

Allig

ator R

idg

e

0 10 20

km

Figure 2. Map of the same area as Plate 1, showing relevant geographic names, includ-ing ranges, valleys, towns, peaks, roads, and county boundaries (abbreviations: R.—range, Mtn.—mountain, Mts.—mountains, Vly.—valley).

1Supplemental File. Zipped fi le containing three supplemental fi gures, a word document, and a zipped fi le containing an ArcGIS MXD and accompanying shape fi les. If you are viewing the PDF of this paper or reading it offl ine, please visit http:// dx .doi .org /10 .1130 /GES01102 .S2 or the full-text article on www .gsapubs .org to view the Supplemental File.



combined with subcrop patterns to estimate structural relief and fold amplitude requires assuming that topographic relief was small rela-tive to structural relief during the Paleogene; and (3) the subcrop map does not remove the horizontal effects of postunconformity tecto-nism, including translation that accompanied Neogene extension.

Dip Magnitude Maps

Dip magnitude maps of the same area as Plate 1, which show present-day attitude, color coded by dip direction and dip angle, are shown for Tertiary rocks and Paleozoic–Mesozoic rocks in Figures 3A and 3B, respectively. These maps were constructed by compiling over 4200 bed-ding measurements from the geologic maps cited on Plate 1, and they highlight areas where multiple attitude measurements demonstrate that Tertiary or Paleozoic–Mesozoic rocks have a consistent attitude. Strike and dip symbols shown on Figure 3A represent the mean attitude of multiple measurements, which are shown in individual stereoplots in Figure SM1 in the sup-plemental fi le (strike and dip data for Paleozoic–Mesozoic rocks are shown in Fig. SM2 in the supplemental fi le [see footnote 1]). The Paleo-zoic–Mesozoic dip magnitude map (Fig. 3B) corroborates the mapping and regional correla-tion of folds performed on Plate 1, and it allows quantitative description of present-day fold limb dips, which are summarized in Table 1.

In 71 locations, Paleozoic–Mesozoic rocks were restored to their Paleogene attitude by rotating the mean attitude of Tertiary rocks to horizontal, and rotating Paleozoic–Meso-zoic rocks by the same amount. The resulting Paleogene attitudes are shown as strike and dip symbols on Plate 1 and Figure 3C. Though they

are distributed across a large region, these data provide quantitative estimates of the local pre-extensional limb dip magnitudes of folds, which are summarized on Table 1. In addition, histo-grams plotting the difference in dip angle across

the Paleogene unconformity within the Eastern Nevada fold belt and Central Nevada thrust belt are shown on Figure 4, and include an additional 17 data points calculated from the subcrop map of Gans and Miller (1983).

540°0

0’N

39°3

0’N

39°0

0’N

38°3

0’N

38°0

0’N

115°30’W116°00’W

115°00’W

A Tertiary rocks: present day attitude

25

0°–20°21°–40°41°–60°61°–>90°

0°–20°21°–40°41°–60°61°–>90°

Dip toward east:

Dip toward west:

Attitude symbols:

dipping 1–90°

horizontal10 from Stewart

(1980, Fig. 51)

0 10 20

km

22

16

19

~8

22

14

12

2417

17231514

13

12

34

38

37

35

30

3633

43

36

25

17

19 1916

19

11

17

12

23

~23

~

~

~5~3

712

~9 19

15

21

2825

21

97

21

1525

26

28

28

29

18

17

29

26

28

20

18

2428

44

28

1217

12~

~

~~

~

18

172114

10

30

25

10

<5

1

4

21

31

65

72

75

78

97

105107

110114

117

119

120122

123127

128

129

130

131

132

133

134

136

138

140

142 143

144

146 148150

153155 159161

167

170

179

182

184

187

189

191

193

202

196 198

207

212

215

217219

220

221

222

224226

228230

239

244

246

248 250

252

Figure 3 (on this and following page). Dip magnitude maps of the same area as Plate 1 (see Plate 1 for structure abbreviations). Col-ored polygons represent areas on source map-ping where multiple attitude measurements demonstrate that rocks consistently have a similar attitude. Areas with variable attitude or insuffi cient attitude data are not shown. (A) Dip magnitude map showing present-day attitudes of Tertiary rocks. Strike and dip symbols represent the mean attitude of mul-tiple measurements, which are plotted on Fig-ure SM1 (see text footnote 1); brown numbers next to strike and dip symbols correspond to individual stereoplots in Figure SM1 (see text footnote 1).

Long


GST

PTS

SRS

DT

MSS

MPT

TSA

BFS

SMT

RT

TMA SCT

Butte

synclinorium

Illipah

anticline

LAS

ST

ATRMT

RMTEC

EC

Pinto

Creek

syncline

HFS

DTF

PSFMNT

PMT

Cherry

Creek

anticline

?

40°0

0’N

39°3

0’N

39°0

0’N

38°3

0’N

38°0

0’N

115°00’W116°00’W

B Paleozoic-Mesozoic rocks: present day attitude

0°–20°21°–40°41°–60°61°–>90°

0°–20°21°–40°41°–60°61°–>90°

Dip toward east:

Dip toward west:

0 10 20

km

GST

PTS

SRS

DT

MSS

MPT

TSA

BFS

SMT

RT

TMA SCT

Butte

synclinorium

Illipah

anticline

LAS

ST

AT

RMT

RMTEC

EC

Pinto

Creek

syncline

HFS

DTF

PSF

MNT

PMT

Cherry

Creek

anticline

40°0

0’N

39°3

0’N

39°0

0’N

38°3

0’N

38°0

0’N

115°00’W115°30’W116°00’W

C Paleozoic-Mesozoic rocks: Paleogene attitude

25

0°–20°21°–40°41°–60°61°–>90°

0°–20°21°–40°41°–60°61°–>90°

Dip toward east:

Dip toward west:

Attitude symbols:dipping 1–90°horizontal

0 10 20

km

14

43

22

3751 12

19

311414

66

63

6169

53

23

18 1726

33

15

26 49

12

36 9

30

2212

108

26

29

6

15

18

26

36

7

11

17

13

58 1011

19

4

411

3

31

8

11

14

30 9

4024

6

21

26

12

13 33

399

45

281357

Figure 3 (continued ). (B) Dip magnitude map showing present-day attitudes of Paleozoic and Mesozoic rocks. Strike and dip sym-bols are omitted here for simplicity; strike and dip symbols referenced to specific stereoplots are shown in Figure SM2 in the Supple-mental File (see text footnote 1). First-order folds of the Eastern Nevada fold belt are emphasized by thick fold symbols. (C) Dip magnitude map showing Paleogene attitudes of Paleozoic and Mesozoic rocks, calculated by rotating Tertiary rocks to horizontal, and rotating Paleozoic–Mesozoic rocks in that locality by the same amount. See Plate 1 for a guide to stereoplots referenced to Fig-ure SM1 (see text footnote 1) for each attitude symbol. First-order folds of the Eastern Nevada fold belt are emphasized by thick fold symbols.



Pre-Extensional Tectonic Reconstruction Base Map

On Figure 5, the locations of thrust faults, fold axes, and the boundaries of structural prov-inces compiled from Plate 1 and from published subcrop and geologic maps (Gans and Miller, 1983; Colgan and Henry, 2009; Colgan et al., 2010; Long, 2012; Greene, 2014) are super-imposed over a base map containing polygons from McQuarrie and Wernicke (2005, their fi g. 7A), which shows present-day map dimensions. On Figure 6, these structures and provinces are superimposed over a base map containing poly-gons from McQuarrie and Wernicke (2005, their Fig. 9E), which shows a regional tectonic recon-struction of extension at 36 Ma. The locations of structures and province boundaries on Figure 6 were taken directly from their locations on the range polygons of Figure 5. Therefore, Figure 6 illustrates the approximate synorogenic dimen-sions of individual structures and structural provinces, and it facilitates estimation of the pre-extensional wavelength of folds, which are summarized on Table 1. It is acknowledged that estimation of the amount of Cenozoic extension across the Great Basin is an ongoing process and will undoubtedly be refi ned with future research; however, the McQuarrie and Wernicke (2005) reconstruction is the most recent and comprehensive tectonic reconstruction avail-able to date.

STRATIGRAPHY

Plate 1 shows that rocks ranging between Cambrian and Cretaceous in age were exposed at the surface during the Paleogene. The Cam-brian through Triassic rocks are part of a com-posite sedimentary section that records semi-continuous deposition from the Neoproterozoic to the Triassic (e.g., Stewart, 1980). From Late Neoproterozoic to Devonian time, a westward-thickening section of clastic and carbonate rocks that approaches thicknesses of 10 km was deposited on the rifted western Laurentian conti-nental shelf in western Utah and eastern Nevada (e.g., Stewart and Poole, 1974). The lower part of the section consists of >5 km of Neoprotero-zoic to Early Cambrian clastic rocks (Stewart , 1980). These rocks are presently exposed in several deeply exhumed ranges in western Utah and eastern Nevada (Stewart and Carlson, 1978; Hintze et al., 2000); however, Paleogene erosion levels were not deep enough to expose these rocks anywhere on Plate 1. The Middle Cambrian through Devonian section represents the upper ~4–5 km of the passive-margin basin (Stewart, 1980) and is dominated by carbonate rocks. On the area of Plate 1, Cambrian rocks

TAB

LE 1

. DA

TA F

OR

FO

LDS

OF

TH

E E

AS

TE

RN

NE

VA

DA

FO

LD B

ELT

, CE

NT

RA

L N

EV

AD

A T

HR

US

T B

ELT

, AN

D W

ES

TE

RN

UTA

H T

HR

US

T B

ELT

Str

uctu

reP

aleo

gene

ero

sion

leve

l of w

este

rn li

mb

Pal

eoge

ne e

rosi

onle

vel o

f eas

tern

lim

bD

efor

mat

ion

timin

g co

nstr

aint

sM

oder

n w

este

rnlim

b di

pM

oder

n ea

ster

nlim

b di

pC

entr

al N

evad

a th

rust

bel

tc d

Mot

pO

*noit animluc

akeruE

†C

hs to

Pcr

†E°07–04

W°51–01*cn

K-nys;naitpA

McC

lure

Spr

ing

sync

line#

Ddg

to P

rh, K

ncD

dg to

Prh

, Knc

fold

s P

rh; c

ut b

y un

date

d K

nc#

25–4

0°E

(≥9

0°E

# )un

know

n (5

0°W

# )Tr

ap S

prin

g an

ticlin

e††hr

Psdlof

ePI

otgd

Dc n

K,hrP

otgd

D#

unkn

own

unkn

own

Bac

on F

lat s

yncl

ine††

W°53–02n

wonknue

PIsdlof

ePI

otn

De

PIot

gdD

Eas

tern

Nev

ada

fold

bel

t: F

irst-

orde

r fo

lds

ot°03

*cnK

naitpA

sdlofcn

K,rcP

otgd

Dc n

K, rcP

otc

Men ilcnys

k eerC

o tn iP

≥90°

E20

–50°

W E°04–02W°53–02

tm

RT

sdloft

mR

Tot

g dD

hrP/rc

Pot

g dD

e nilc it nah ap ill I

ot°52E°05–02

tm

RT

sdloft

mR

Tot

pdM

tm

RT

otgd

Dmuironilcnys

ettuB

≥90°

Wc issaruJ

rewo L

otpd

Mt

mR

Tot

pdM

enilcitnakeer

Cy rreh

C††

†fo

lds

Low

er J

uras

sic

rock

s§§§

25–3

0°W

unkn

own

cissaruJre

woLot

pdM

muironilcnyspouqe

P††

†M

iss.

to L

ower

Jur

assi

c††fo

lds

Low

er J

uras

sic

rock

s§§§

unkn

own

unkn

own

Wes

tern

Uta

h th

rust

bel

tC

onfu

sion

syn

clin

oriu

m**

**M

iss.

To

Low

er T

riass

ic††

†Tr

iass

ic a

nd d

eepe

r††††

fold

s Lo

wer

Tria

ssic

roc

ks50

°to ≥9

0°E

††††

15–4

0°W

††††

Eas

tern

Nev

ada

fold

bel

t: S

econ

d-or

der

fold

s

Loca

tion/

stru

ctur

eR

ange

of P

aleo

gene

eros

ion

leve

ls in

lim

bsA

ge c

onst

rain

tsR

ange

of

mod

ern

limb

dips

Ran

ge o

f P

aleo

gene

lim

b di

psR

ange

of

ampl

itude

s (m

)0 051–0 05

nwonk nu

°08–52cn

Kd et adnu

dnarc

Pdlo f

cnK,rc

Pot

ePI

.stM

dnomai

Dnrehtro

N0501 –006

E°55–01E°56–02

aP

sdl ofa

Po tjp

DM

enilcnysepoletn

Ael ttiL

006–003n

wonknu°04–52

ePI

dlofe

PIot

pdM

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eniP

etihW

nrehtroN

007–052n

wonknu°03–51

tm

RT

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mR

Tot

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C(c

ontin

ued

)

Long


were only exposed in the Fish Creek Range, and include the Secret Canyon Shale, Hamburg Dolomite, Dunderberg Shale, and Windfall For-mation (see Plate 1 for a correlation chart of map units). Ordovician rocks were exposed in the Fish Creek, Antelope, Pancake, and Quinn Canyon Ranges and consist of the limestone-dominated Pogonip Group, the Eureka Quartz-ite, and the Hanson Creek Dolomite. The Silu-rian section consists of the Lone Mountain Dolomite. Devonian rocks are divided into the lower and upper Nevada Formation, which is dominated by dolomite, the Guilmette Forma-tion/Devil’s Gate limestone, and the Pilot Shale.

During the Mississippian Antler orogeny, up to ~2–3 km of conglomerate, shale, and sand-stone were deposited in a foreland basin that subsided to the east of an orogenic highland produced from east-vergent contractional defor-mation (e.g., Poole, 1974; Poole and Sandberg, 1977; Speed and Sleep, 1982). The western third of Plate 1, immediately east of the trace of the Roberts Mountains thrust, was the approxi-mate axis of maximum subsidence in the fore-land basin (Stewart, 1980). Mississippian rocks of the Antler foreland basin include the Dale Canyon Formation, Chainman Shale, and Dia-mond Peak Formation.

After the Antler orogeny, ~2–4 km of Pennsyl-vanian to Triassic, dominantly shallow-marine carbonate rocks were deposited on the conti-nental shelf (Rich, 1977; Stevens, 1977; Col-linson and Hasenmueller, 1978; Stewart, 1980). Eastern Nevada experienced a protracted series of uplift and erosion events during the Pennsyl-vanian and Permian (Trexler et al., 2004), which are recorded by several unconformities within this part of the section. The Pennsylvanian sec-tion consists of the Ely Limestone; the Permian section consists of the Garden Valley Forma-tion, Carbon Ridge Formation, and Rib Hill Sandstone, which are laterally equivalent (Hose and Blake, 1976; Roberts et al., 1967), and the Arcturus Formation and Park City Group. The Triassic section consists of the Thaynes and Moenkopi Formations.

The Early Cretaceous Newark Canyon Formation is preserved in several isolated exposures in the western part of Plate 1, unconformably overlying Mississippian, Penn-sylvanian, and Permian rocks. The Newark Canyon Formation has been interpreted to represent deposition contemporary with con-tractional deformation in the Central Nevada thrust belt (Vandervoort and Schmitt, 1990; Druschke et al., 2010; Long et al., 2014). At its type section in the southern Diamond Mountains, the Newark Canyon Formation has been dated as Aptian (ca. 122–116 Ma) by U-Pb zircon geochronology (Druschke et al.,

TAB

LE 1

. DA

TA F

OR

FO

LDS

OF

TH

E E

AS

TE

RN

NE

VA

DA

FO

LD B

ELT

, CE

NT

RA

L N

EV

AD

A T

HR

US

T B

ELT

, AN

D W

ES

TE

RN

UTA

H T

HR

US

T B

ELT

(co

ntin

ued

)

Str

uctu

reP

aleo

gene

wes

tern

lim

b di

pP

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2010), and deposition in the Fish Creek Range can be narrowed to the Barremian-Albian (ca. 130–100 Ma) on the basis of biostratigraphy (Fouch et al., 1979; Hose, 1983). However, rocks mapped as Newark Canyon Formation in several localities in the Pancake Range (McDonald , 1989; Carpenter et al., 1993; Perry and Dixon, 1993) and in the northern Diamond Mountains (Stewart and Carlson, 1978) lack precise depositional age constraints.

CONTRACTIONAL STRUCTURES

The following sections discuss the map pat-terns and geometry of regional-scale folds and thrust faults of the Eastern Nevada fold belt, Central Nevada thrust belt, and Western Utah thrust belt. Several structures discussed here, such as the Butte synclinorium and Eureka culmination, have been described in previous studies; however, many folds and thrust faults are named, described, and regionally correlated for the fi rst time here. Data on Paleogene ero-sion levels, geometry, and deformation timing constraints for folds and thrust faults are sum-marized in Tables 1 and 2, and detailed descrip-tions of how these structures were mapped, correlated, and defi ned on the basis of source mapping are included in the Supplemental File (see footnote 1). In most cases, the pre-Paleogene amplitudes of folds were deter-

mined based on the total range of subcrop units exposed in each limb, combined with regional stratigraphic thicknesses from Stewart (1980). In some cases, the amplitudes of folds were estimated from cross sections accompanying source maps. Modern and pre-Paleogene wave-length ranges for folds were estimated from the distance between the axes of adjacent fi rst-order folds on Figures 5 and 6, respectively. Throw ranges on thrust faults were estimated from the stratigraphic levels of the hanging wall and footwall, combined with stratigraphic thicknesses from Stewart (1980).

Roberts Mountains Thrust

The Roberts Mountains thrust, which emplaced deep-water sedimentary rocks over continental shelf rocks during the Mississippian Antler orogeny (e.g., Speed and Sleep, 1982; Burchfi el and Royden, 1991), is exposed in the western part of Plate 1. North of Devil’s Gate, the Roberts Mountains thrust places the Ordo-vician Vinini Formation over Devonian and Mississippian rocks. During the Paleogene, the Permian Garden Valley Formation, which strati-graphically overlaps the Roberts Mountains thrust, was exposed across much of the north-west corner of the map area. In the southern Fish Creek Range, the Devonian Woodruff For-mation is exposed in a klippe above the Roberts

Mountains thrust, overlying Mississippian rocks (Stewart and Poole, 1974; Stewart and Carlson, 1978; Stewart, 1980; Hose, 1983).

Eastern Nevada Fold Belt

The Eastern Nevada fold belt is defi ned as the 100–150-km-wide region between the Cen-tral Nevada thrust belt and Western Utah thrust belt (Fig. 5), which restores to a pre-extensional width of 50–100 km (Fig. 6). Five north-trend-ing folds within this province can be traced for map distances between 100 and 250 km, with amplitudes of ~2–4 km and wavelengths of ~20–40 km, and are classifi ed here as fi rst-order folds (Table 1). In several areas, including the northern Diamond Mountains (Haworth, 1979; Larson and Riva, 1963), central White Pine Range (Humphrey, 1960; Guerrero, 1983), and southern Butte Mountains (Douglass, 1960), subsidiary, second-order folds are present, and they can be traced for map distances typically ≤10 km, have amplitudes typically ≤1 km, and have wavelengths of ~1–10 km (Table 1). The fi ve fi rst-order folds of the Eastern Nevada fold belt are described next, from west to east.

Pinto Creek SynclineA syncline that preserves rocks as young as

Permian and Cretaceous in its hinge zone can be traced for ~95 km through the Diamond Moun-tains and the northern Pancake Range (Plate 1). The portion of this fold in the southern Diamond Mountains was named the Pinto Creek syncline (Nolan et al., 1974), and this name is applied here to its full length. In the Diamond Moun-tains, the eastern limb dips 20°–40° west, and the dip of the western limb varies between 25°E to 80°W (overturned). In the Pancake Range, the eastern limb dips 20°W, and the western limb dips 15°E. Retrodeformation of tilts of Tertiary rocks indicates original western and eastern limb dips of 20°–30°E and 30°–40°W, respectively, although areas of the western limb may have dipped as steeply as 80°E (Table 1). The amplitude of the Pinto Creek syncline is between 1400 and 3000 m, and the pre-Paleo-gene wavelength was 25–35 km. The syncline folds the Aptian (ca. 116–122 Ma) Newark Can-yon Formation in the southern Diamond Moun-tains (Long et al., 2014), and it folds undated rocks mapped as Newark Canyon Formation in the northern Diamond Range (Stewart and Carlson, 1978). Long et al. (2014) interpreted the portion of the Pinto Creek syncline in the southern Diamond Mountains as the frontal axis of a hanging-wall ramp above the Ratto Canyon thrust, which grew synchronous with Newark Canyon Formation deposition. However, the construction mechanism for this fold farther

0

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0–9° 10–19° 20–29° 30–39°

18

n = 88 71 = this study 17 = Gans and Miller (1983)

Difference in dip angle across Paleogene unconformity40–49° 50–59° 60–90°

3026

20

11

3 5 5

A Eastern Nevada fold belt:

B Central Nevada thrust belt:

C ENFB and CNTB combined

Figure 4. Histograms showing the difference in dip angle between Paleozoic–Mesozoic rocks and Tertiary rocks across the Paleo-gene unconformity, from (A) the Eastern Nevada fold belt; (B) the Central Nevada thrust belt; and (C) for both of these prov-inces combined. Strike and dip symbols showing data from this study are on Plate 1 and Figure 3C, and raw data used in calcu-lating these attitudes are shown in stereo-plots in Figure SM1 (see text footnote 1). Seventeen data points for the Eastern Nevada fold belt were calculated from the subcrop map of Gans and Miller (1983). These data indicate that the pre-Paleogene dip of fold limbs and other areas of homo-clinally dipping rocks within the East-ern Nevada fold belt and Central Nevada thrust belt typically range between 10° and 40°, which is signifi cantly higher than the ≤10°–15° range proposed by early mapping studies (e.g., Young, 1960; Kellogg, 1964; Moores et al., 1968).

Long


north in the Diamond Mountains is unclear, as the geometry changes to a much tighter fold with multiple subsidiary folds, and no thrust faults are exposed through a complete section of Silurian through Permian rocks in its western limb (Nolan et al., 1971).

Illipah AnticlineAn anticline that preserves Mississippian

and Devonian rocks in its hinge zone can be traced for ~105 km through the White Pine Range, Alligator Ridge, and Bald Mountain (Plate 1). The portion of this fold in the north-

ern White Pine Range was named the Illipah anticline (Humphrey, 1960), and this name is applied here to its full length. The western limb dips 20°–35°W, and the eastern limb dip varies between 15°E and 45°E. Retrodeformation of tilts of Tertiary rocks indicates original limb

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37°N

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Figure 5. Map of eastern Nevada and western Utah (location shown on Fig. 1A) showing structural provinces of the Sevier hinterland, superimposed over a base map from McQuarrie and Wernicke (2005, their Fig. 7A) that shows present-day dimensions. Struc-ture abbreviations are shown on Figure 6, except for: REHCC—Ruby–East Humboldt core com-plex, SRCC—Snake Range core complex, and WFW—area inter-preted as exhumed footwall of Windermere thrust (Camilleri and Chamberlain, 1997). For areas that fall outside of the area of Plate 1, the locations of structures are compiled from Long (2012) for the Sevier thrust belt, southern part of the Central Nevada thrust belt, and southern part of the East-ern Nevada fold belt; Gans and Miller (1983) for the eastern part of the Eastern Nevada fold belt; Long (2012), Colgan and Henry (2009), and Colgan et al. (2010) for the northern part of the East-ern Nevada fold belt; and Greene (2014) for the Western Utah thrust belt.



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Structure abbreviations, continued:

CSA - Conger Springs anticline CS - Confusion synclinorium SMT - Salt Marsh thrustEastern Nevada fold belt: PS - Pequop synclinorium CCA - Cherry Creek anticline BS - Butte synclinorium IA - Illipah anticline PCS - Pinto Creek syncline LAS - Little Antelope synclineCentral Nevada thrust belt: GMPTS - Golden Gate-Mount Irish- Pahranagat thrust system RLFTS - Rimrock-Lincoln-Freiberg thrust system BRT - Belted Range thrust ST - Sawmill thrust BCT - Big Cow thrust PMT - Portuguese Mountain thrust AT - Antelope thrust MPT - Moody Peak thrust PTS - Pancake thrust system DT - Duckwater thrust EC - Eureka culmination BFS - Bacon Flat syncline TSA - Trap Spring anticline MSS - McClure Spring synclineOther: RMT - Roberts Mountains thrust IT - Independence thrust SDD - Sevier Desert detachment LVVSZ - Las Vegas Valley shear zone

Structure abbreviations:

Sevier fold-thrust belt: DWCTS - DeLamar-Wah Wah-Canyon Range thrust system PVTS - Pavant thrust system PXT - Paxton thrust GT - Gunnison thrust SRT - Sheeprock thrust SVT - Skull Valley thrust TVT - Tule Valley thrust CNTS - Charleston-Nebo thrust system AT - Absaroka thrust CT - Crawford thrust SC - Sevier culmination KT - Keystone thrust WPT - Wheeler Pass thrust GPT - Gass Peak thrust CLT - Clery thrust SDT - Spotted Range thrustWestern Utah thrust belt: KCT - King’s Canyon thrust BWT - Brown’s Wash thrust

CCA

PMT

DeCelles andCoogan (2006)cross-section

line

approximatecross-section

line of Figure 7

N

36 Ma

Figure 6. Map of eastern Nevada and western Utah, superimposed over a base map from McQuarrie and Wernicke (2005, their Fig. 9E) that shows a 36 Ma tectonic reconstruction. The map shows the approximate pre-extensional dimensions of structural provinces of the Sevier hinterland. The restored locations of all structures are taken from their locations over polygons on Figure 5.

Long


dips between 15°W and 35°W for the western limb, and 15°–30°E for the eastern limb. The amplitude of the Illipah anticline is between 1200 and 3800 m, and its pre-Paleogene wave-length was 35–50 km. Rocks as young as Lower Triassic are folded in the eastern limb, providing a maximum age bound.

Butte SynclinoriumThe Butte synclinorium (Hose, 1977; Gans

and Miller, 1983) preserves rocks as young as Permian and Triassic in its hinge zone and can be traced for 250 km (Fig. 5; Long, 2012). Subcrop patterns of the central part of the synclinorium are shown on Plate 1. In the Butte Mountains, western and eastern limb dips are 20°–30°E and 25°–30°W, respectively. To the south, along Radar Ridge, the master structure of the synclinorium is referred to as the Radar Ridge syncline (Brokaw and Barosh, 1968), and it has a western limb dip of 35°–50°E and an eastern limb dip that varies between 30°W and over-turned. The amplitude of the Butte synclinorium is between 2300 and 3800 m, and its pre-Paleo-gene wavelength was 25–45 km. Rocks as young as Lower Triassic are folded in the hinge zone.

Cherry Creek AnticlineThe subcrop pattern of an anticline that pre-

serves Devonian, Mississippian, and Pennsyl-vanian rocks in its hinge zone was defi ned east of the Butte synclinorium on the subcrop map of Long (2012), and it is here named the Cherry Creek anticline (Fig. 5). The fold can be traced for 110 km, from southern Butte Valley through the Cherry Creek Range and northern Egan Range. The southern 30 km of the anticline axis is present on Plate 1, where the western limb dips 25°–30°W. Retrodeformation of Ter-tiary tilts defi nes a Paleogene western limb dip of 15°–20°W, and data from the subcrop map of Gans and Miller (1983) defi ne a Paleogene eastern limb dip of 10°–35°E. The amplitude of the Cherry Creek anticline is between 2300 and 4000 m, and the pre-Paleogene wavelength was 15–40 km. Rocks as young as Lower Jurassic (Coats, 1987) are folded in the eastern limb.

Pequop SynclinoriumThe Pequop synclinorium (Long, 2012) is

defi ned by a subcrop pattern of Permian, Trias-sic, and Jurassic rocks preserved for a distance of 115 km, from the northern Schell Creek Range to the southern Pequop Mountains (Fig. 5). Paleo-gene limb dips for the southern part of the fold in the Schell Creek Range, estimated from retro-deformed attitudes presented in Gans and Miller (1983), are between 10°E and 35°E in the west-ern limb and 25°–30°W in the eastern limb. The amplitude is between 2500 and 4000 m, and the

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pre-Paleogene wavelength was ≤25 km (Fig. 6). Rocks as young as Lower Jurassic (Coats, 1987) are folded in the hinge zone.

Central Nevada Thrust Belt

The Central Nevada thrust belt is a series of east-vergent thrust faults and folds that accom-modated ~10 km of shortening, and which connect southward with the interior part of the Sevier thrust belt in southern Nevada (Fig. 5; Bartley and Gleason, 1990; Taylor et al., 1993, 2000; Long, 2012; Long et al., 2014). Plate 1 facilitates more detailed description and regional correlation of structures in the northern half of the Central Nevada thrust belt than the lower-resolution subcrop map of Long (2012). Next, descriptions of structures defined in source mapping are presented, several of which are named here.

Eureka Culmination and Associated Structures

The Eureka culmination, an anticline with a wavelength of 20 km, an amplitude of 4.5 km, and limb dips of 25°–35°, was defi ned in retro-deformed cross sections across the northern Fish Creek Range and southern Diamond Mountains (Long et al., 2014). A Cambrian over Silurian relationship defi ned in drill holes under the anticline crest was interpreted as the blind Ratto Canyon thrust, and the culmination was interpreted as a fault-bend fold constructed by 9 km of eastward motion of the Ratto Canyon thrust sheet over a footwall ramp (Long et al., 2014). The type section of the Early Cretaceous (Aptian, ca. 116–122 Ma) Newark Canyon For-mation was deposited in a piggyback basin that developed on the eastern limb of the culmina-tion as it grew (Long et al., 2014). On the basis of deep Paleogene erosion levels, the Eureka culmination can be traced for 80 km.

Within the eastern limb of the Eureka cul-mination, the east-vergent Moritz-Nager thrust (French, 1993) places Devonian rocks over Mis-sissippian rocks (Plate 1). The Moritz-Nager thrust exhibits 1–2 km of displacement and is interpreted as a subsidiary structure that post-dates the majority of motion on the Ratto Can-yon thrust (Long et al., 2014).

After its construction, the Eureka culmina-tion was deformed by normal faults that pre-date late Eocene volcanism (Long et al., 2014), including (from east to west) the Pinto Summit fault, Hoosac fault system, and Dugout Tun-nel fault (Plate 1). The youngest prevolcanic normal faulting was accompanied by eastward tilting, which steepened the eastern limb dip to 60°–70°E, and shallowed the western limb dip to 15°–20°W (Fig. 3B).

Antelope ThrustIn the northern Antelope Range, the east-

vergent Antelope thrust (Carpenter et al., 1993) places Ordovician rocks over Mississippian rocks (Hose, 1983) and is correlated to the south with a thrust fault mapped in the Park Range that places Devonian rocks over Pennsylvanian–Permian rocks (Dixon et al., 1972). Throw on the Antelope thrust is 2600 m in the Antelope Range, and this decreases to 900–1400 m in the Park Range.

Northern Pancake RangeDifferent names for folds and thrust faults

in the northern Pancake Range have been pro-posed (Nolan et al., 1974; Carpenter et al., 1993; Ransom and Hansen, 1993; Long, 2012). Here, a new naming scheme is proposed, based on primary map sources (Nolan et al., 1974; McDonald, 1989), with additions from Carpen-ter et al. (1993).

The Moody Peak thrust (Carpenter et al., 1993) places Ordovician and Silurian rocks over Devonian rocks in the northwest corner of the range (Kleinhampl and Ziony, 1985), and it has an estimated throw of 700–1750 m. Carpenter et al. (1993) stated that the Moody Peak thrust cuts undated rocks mapped as the Newark Can-yon Formation. However, given the diffi culties in correlating rocks without precise age control that are mapped as Newark Canyon Forma-tion (see discussion in “Stratigraphy” section), the Early Cretaceous maximum motion age constraint that this fi eld relationship implies is considered tentative. The Moody Peak thrust and Ratto Canyon thrust are correlated here, based on their spatial relationships to the deep Paleogene erosion levels of the Eureka culmi-nation, and the relative stratigraphic levels that they deform.

The Pancake thrust system, defi ned here by correlating thrust faults in the northwest Pan-cake Range described by Nolan et al. (1974), McDonald (1989), and Carpenter et al. (1993), can be traced for 35 km (Plate 1), and throw on individual structures varies from 300 to 1300 m. Structures of the Pancake thrust system cut rocks as young as Mississippian and are truncated by an Aptian (108 ± 3 Ma, K-Ar biotite; Nolan et al., 1974) dacite stock (McDonald, 1989).

The Green Springs thrust (McDonald, 1989) places Devonian and Lower Mississippian rocks over Upper Mississippian rocks, corresponding to 600–1500 m of throw. Undated conglomer-ate mapped as the Newark Canyon Formation overlaps the Green Springs thrust (McDonald, 1989); however, similar to the discussion for the Moody Peak thrust, without precise age con-trol on these rocks, this motion age constraint should be considered tentative.

The Duckwater thrust (Carpenter et al., 1993) places Devonian and Lower Mississippian rocks over Upper Mississippian, Pennsylvanian, and Permian rocks (Plate 1), corresponding to 1500–2100 m of throw. The Duckwater thrust can be traced for 30 km, and it is speculatively traced northward into Newark Valley on the basis of subcrop patterns.

Central Pancake Range and Railroad ValleySubcrop patterns in Railroad Valley were

aided by drill-hole data from petroleum explo-ration (Hess et al., 2004). In most areas, subcrop patterns were interpreted as representing ero-sionally beveled folds, based on a lack of older over younger structural relationships observed in Railroad Valley drill holes (French, 1998).

A northeast-striking, east-vergent thrust fault mapped in the central Pancake Range (Quinli-van et al., 1974) is here named the Portuguese Mountain thrust. This fault places Devonian and Lower Mississippian rocks over Upper Missis-sippian rocks, corresponding to a throw range of 250–1350 m.

The McClure Spring syncline (Perry and Dixon, 1993) preserves Mississippian, Penn-sylvanian, and Permian rocks in its hinge zone. West of Duckwater, the fold has a vertical to overturned western limb and an eastern limb that dips as steep as 50°W, and it is interpreted as east-vergent (Perry and Dixon, 1993). Here, undated rocks mapped as the Cretaceous New-ark Canyon Formation are preserved in its hinge zone (Kleinhampl and Ziony, 1985); however, Perry and Dixon (1993) argued that Permian rocks are the youngest involved in folding. In the southern part of the fold, the western limb dips 25°–40°E and restores to a Paleogene dip of 10°–15°NE. The amplitude of the syncline varies from 1100 to 2600 m along its length.

An anticline can be traced through Railroad Valley and the central Pancake Range on the basis of an elongated subcrop pattern of Devo-nian rocks (Plate 1). This fold was originally defi ned in Railroad Valley by French (1998), and it is here named the Trap Spring anticline because of its proximity to the Trap Spring oil fi eld. The amplitude ranges from 600 to 1300 m in Railroad Valley to a maximum of 2600 m where Permian rocks are preserved in its western limb.

A syncline can be traced along the eastern side of Railroad Valley and through the Duck-water Hills, on the basis of an elongated subcrop pattern preserving rocks as young as Pennsyl-vanian (Plate 1). This syncline was originally defi ned in Railroad Valley by French (1998), and it is referred to here as the Bacon Flat syn-cline, after its proximity to the Bacon Flat oil fi eld. Its amplitude varies from 600 to 1500 m.

Long


Quinn Canyon Range and Southern Grant Range

Three thrust faults are mapped in the Quinn Canyon and Grant Ranges, and they are listed here from structurally highest to lowest.

The Sawmill thrust (Bartley and Gleason, 1990) places Ordovician rocks over Devo-nian rocks, corresponding to a throw range of 1250–3050 m. The Sawmill thrust can be traced for 20 km, and it cuts rocks as young as Upper Devonian.

The Rimrock thrust (Bartley and Gleason, 1990) is the northernmost segment of the Rim-rock-Lincoln-Freiberg thrust system (Fig. 5), which connects southward with structures of the Sevier thrust belt (Taylor et al., 2000; Long, 2012). The Rimrock thrust places Lower and Middle Devonian rocks over Upper Devonian rocks (Ekren et al., 2012), corresponding to a throw of 650–1200 m. Thirty kilometers south of Plate 1, structures associated with the cor-relative Lincoln thrust cut rocks as young as Pennsylvanian, and they are crosscut by a Late Cretaceous (ca. 90–98 Ma; K-Ar biotite) granite pluton (Taylor et al., 2000).

The Schofi eld Canyon thrust places Cam-brian rocks over Ordovician rocks, and it has an estimated throw of 2700 m (Fryxell, 1988, 1991). Based on subcrop data, the Schofi eld Canyon thrust was not erosionally breached by the Paleogene (Plate 1). The Timber Mountain anticline, a recumbent hanging-wall fold, is interpreted to be genetically related to motion on the Schofi eld Canyon thrust (Fryxell, 1988). The axis of the anticline is crosscut by the Late Cretaceous (86.4 ± 4.6 Ma; U-Pb zircon) Troy granite stock (Taylor et al., 2000).

Western Utah Thrust Belt

Recent work in the Confusion Range in west-ern Utah (Greene, 2014) has defi ned the West-ern Utah thrust belt, a 150-km-long system of surface-breaching, east-vergent thrust faults that branch off of the Sevier thrust belt (Fig. 5), deform Ordovician to Triassic rocks, and col-lectively accommodated ~10 km of shortening. The Confusion synclinorium (Fig. 5), a 130-km-long, north-trending structural trough that pre-serves rocks as young as Triassic in its hinge zone (Hose, 1977), and has long been interpreted as a regional-scale syncline (Gans and Miller, 1983; Long, 2012), has recently been shown to represent a structural low formed by a combina-tion of folding above Western Utah thrust belt thrust faults (Greene, 2014) and construction of the Sevier culmination, a structural high to the east (Allmendinger et al., 1986; DeCelles et al., 1995). The Confusion synclinorium has a western limb dip between 50°E and over-

turned and an eastern limb dip between 15°W and 40°W (Greene, 2014). The western limb of the Confusion synclinorium has an amplitude of 2500–3000 m (Long, 2012; Greene, 2014). Deformation in the Western Utah thrust belt is Triassic or younger, on the basis of the young-est rocks involved in folding, but it is suggested to have been contemporary with Cretaceous to Paleocene shortening in the Sevier thrust belt (Greene, 2014).

DISCUSSION

Eastern Nevada Fold Belt: Absence of Thrust Faults and Deep Décollement Interpretation

The Eastern Nevada fold belt is characterized by fi ve fi rst-order folds that can be traced for distances between 100 and 250 km, with typi-cal limb dips of 10°–30°, amplitudes of 2–4 km, and pre-extensional wavelengths of 20–40 km. For comparison, fi rst-order folds in the Valley and Ridge Province in the north-central Appa-lachians can be traced for 200–300 km, have amplitudes of 5–7 km, and have wavelengths typically ≥12 km (Nickelsen, 1963; Faill, 1998).

The Eastern Nevada fold belt is differenti-ated from the Central Nevada and Western Utah thrust belts by an absence of regional-scale thrust faults or décollement horizons at modern levels of exposure. Within the portion of the Eastern Nevada fold belt on Plate 1, several of the older source maps, including Humphrey (1960) in the White Pine Range, Fritz (1968) in the Cherry Creek Range, and Brokaw and Barosh (1968) in the Egan Range, map structures with modern low dip angles that place younger rocks over older rocks as thrust faults. Gans and Miller (1983), in their classic assessment of extensional style in eastern Nevada, reinterpreted these thrust faults in the Cherry Creek and Egan Ranges as series of highly rotated, domino-style normal faults. In this study, this interpretation is similarly applied to the thrust faults mapped by Humphrey (1960) in the White Pine Range, after the pioneering work of Moores et al. (1968) located 12 km to the south.

East- and west-vergent thrust and reverse faults that do exhibit older over younger rela-tionships, with throw, and in some cases off-set estimates on accompanying cross sections, on the order of tens to hundreds of meters, are mapped in several areas of the Eastern Nevada fold belt on Plate 1, including the southern Dia-mond Mountains (Nolan et al., 1971, 1974), Bald Mountain (Nutt, 2000; Nutt and Hart, 2004), the central White Pine Range (Hum-phrey, 1960), the Grant Range (Lund et al., 1987; Camilleri, 2013), and the Butte Moun-

tains (Otto, 2008). However, these faults can typically only be traced for map distances of 1–5 km, are not traceable across individual source maps or onto adjacent source maps, and can in no cases be correlated regionally. There-fore, on the basis of their modest throw and map extent, they are interpreted as second-order faults that accompanied fi rst-order folding. East of the area of Plate 1, in the Egan, Schell Creek, and Snake Ranges, Gans and Miller (1983) sim-ilarly observed that the primary contractional structures are regional-scale folds, and that no regional-scale thrust faults or décollement hori-zons are present.

The present-day range of stratigraphic levels exposed in the Eastern Nevada fold belt on Plate 1 ranges from Cambrian to Triassic, cor-responding to paleodepths up to 8 km below the Paleogene unconformity. Thick sections of Paleozoic rocks that are undisturbed by faults are observed in the limbs of several fi rst-order folds, including straight sections from Silurian to Permian rocks in the western limb of the Pinto Creek syncline (Larson and Riva, 1963; Nolan et al., 1971), from Mississippian to Trias-sic rocks in the eastern limb of the Butte syn-clinorium (Douglass, 1960; Brokaw and Barosh, 1968), and from Cambrian to Pennsylvanian rocks in the Cherry Creek Range (Fritz, 1968). East of Plate 1, up to 4 km of Neoproterozoic to Lower Cambrian clastic rocks are exposed in the Cherry Creek, Egan, Schell Creek, Snake, and Deep Creek Ranges (Woodward, 1962; Young, 1960; Stewart, 1980; Gans and Miller, 1983), corresponding to paleodepths up to 12 km below the Paleogene unconformity.

On the basis of their approximately uniform amplitude and wavelength over along-strike distances exceeding 100 km, it is proposed here that the fi rst-order folds of the Eastern Nevada fold belt were produced through décollement-style tectonics above a blind, low-angle fault or shear zone that underlies the entire region. One likely candidate is the basal décollement of the Sevier thrust belt, which must transfer 220 km of displacement westward to deeper struc-tural levels under the hinterland (DeCelles and Coogan, 2006). However, the recent recog ni tion of 10 km of upper-crustal shortening accommo-dated in the Western Utah thrust belt (Greene, 2014) indicates the possibility of multi ple décolle ment levels at depth (see discussion in section on “Model for Cordilleran Deformation in the Sevier Hinterland at 39°N”).

The specifi c deformation processes at depth that produced the fi rst-order folds of the Eastern Nevada fold belt are diffi cult to constrain with-out a more precise analysis of their geometry in cross section. A lack of signifi cant steps in structural level across the Eastern Nevada fold



belt implies a regional décollement with rela-tively low structural relief, which makes fault-bend folding an unlikely formation mechanism for the fi rst-order folds. Also, the possibility that these folds represent fault-bend folds above deep-seated duplexes, perhaps constructed from detached basement thrust sheets, as observed in several localities in the Sevier thrust belt in Utah (Allmendinger et al., 1983; DeCelles, 1994; DeCelles et al., 1995; Camilleri et al., 1997; DeCelles and Coogan, 2006), is not favored by the typical 50–100 km along-strike dimensions of these basement-cored culmina-tions (DeCelles, 2004). Instead, the uniform wavelength, amplitude, and map distance of these folds implies that the primary controlling mechanism was the mechanical stratigraphy of the Neoproterozoic to Mesozoic section through which deformation propagated. On this basis, two likely genetic origins for the fi rst-order folds of the Eastern Nevada fold belt are: (1) fault-propagation folds (e.g., Suppe and Medwedeff, 1990) that formed above splays off of the basal décollement that tip out prior to reaching mod-ern levels of exposure, similar to observations in the north-central Appalachian Valley and Ridge Province (e.g., Gwinn, 1970; Kulander and Dean, 1986; Faill, 1998); or (2) detach-ment folds (e.g., Mitra, 2003) that formed above a deep décollement, such as observed in the Zagros fold-and-thrust belt (e.g., Colman-Sadd, 1978; McQuarrie, 2004; Molinaro et al., 2005). Construction of precise fold geometries in a retrodeformed cross section across the Eastern Nevada fold belt will be necessary to distinguish between these folding mechanisms, to estimate depth to decollement using excess area tech-niques (e.g., Epard and Groshong, 1993), and to accurately estimate crustal shortening, which are goals of future work.

Model for Cordilleran Deformation in the Sevier Hinterland at 39°N

Figure 7 shows a generalized, pre-extensional cross section through the Sevier thrust belt and hinterland region at ~39°N. The cross section is used to support the following discussion, which presents a general structural model for Cordi-lleran deformation at this latitude.

In west-central Utah, the Sevier thrust belt accommodated ~220 km of upper-crustal shortening, distributed among a series of thrust faults that breach the surface over an ~50 km across-strike distance (DeCelles and Coogan, 2006). The Canyon Range thrust, the west-ernmost and structurally highest fault, carries as much as 6 km of Neoproterozoic to Lower Cambrian clastic rocks, as indicated by drill-hole data (DeCelles and Coogan, 2006) and the

Consortium for Continental Refl ection Profi ling (COCORP) seismic line (Allmendinger et al., 1983, 1987). The Canyon Range thrust sheet is broadly folded under the House Range, form-ing the Sevier culmination, an anticlinal dome defi ned by Paleozoic subcrop patterns (Harris, 1959; Hintze and Davis, 2003; Long, 2012) and arched refl ectors on the COCORP line (All-mendinger et al., 1983), interpreted as a duplex cored by thrust sheets of Precambrian base-ment rock (Allmendinger et al., 1987; DeCelles and Coogan, 2006). Frontal structures of the Sevier thrust belt, including the Pavant thrust, Paxton thrust, and Gunnison thrust, are inter-preted to root beneath the culmination (DeCelles and Coogan, 2006). Therefore, under the west-ern House Range, which is the farthest point that Sevier thrust faults can be confi dently traced on the COCORP line (Allmendinger et al., 1983), there are at least two décollement levels that together must accommodate the total 220 km of Sevier displacement (Fig. 7). These structures both carry rocks that are deeper than modern exposure levels in eastern Nevada.

In the Confusion Range, the Western Utah thrust belt accommodated ~10 km of shortening, which is distributed between a basal décolle-ment in Ordovician rocks and subsidiary splay-ing thrust faults that ramp up section toward the east and deform rocks as young as Triassic (Greene, 2014). The Western Utah thrust belt defi nes an additional detachment level that roots under the Eastern Nevada fold belt, which must ramp rapidly down section toward the west, through at least 6 km of Neoproterozoic to Cam-brian clastic rocks that are presently exposed in ranges in eastern Nevada (Fig. 7; Stewart, 1980; Gans and Miller, 1983).

Modern exposure levels indicate that a regional décollement that could have produced the fi rst-order folds of the Eastern Nevada fold belt must lie at a minimum depth of 12 km below the top of the Triassic section, corresponding to ~10 km below the Paleogene unconformity (Fig. 7). Under the Eastern Nevada fold belt, the geometry and stratigraphic levels of the basal Sevier décollement and Western Utah thrust belt detachment level are unknown; it is possible that they merge into the same master décollement horizon or shear zone. The contact between Neoproterozoic sedimentary rocks and Pre-cambrian crystalline basement rocks, which is the same exploited by the Canyon Range thrust to the east, is a likely mechanical boundary for localizing such a shear zone; however, involve-ment of Precambrian crystalline basement can-not be ruled out.

During the Late Cretaceous (ca. 70–90 Ma), in the Egan, Schell Creek, and Snake Ranges, Neoproterozoic to Lower Cambrian rocks expe-

rienced regional metamorphism, synchronous with intrusion of granite bodies (Miller and Gans, 1989). This metamorphism was accom-panied by penetrative, top-to-the-east simple shear in rocks as shallow as Lower Cambrian (paleodepths of ~7–8 km; Fig. 7), which increases in intensity down section into Neo-protero zoic rocks (Miller and Gans, 1989). These shear fabrics are synchronous with short-ening in the Sevier thrust belt, and they are inter-preted as a consequence of thermal weakening of the upper crust that accompanied the rise of anatectic melts (Miller et al., 1988; Miller and Gans, 1989). The temporal relationship between this shallow penetrative deformation and con-struction of fi rst-order folds of the Eastern Nevada fold belt is unclear, but these observa-tions indicate that at a late stage in the Cordi-lleran shortening history, the Sevier thrust belt was rooted westward into a diffuse shear zone that affected the base of the upper crust (Miller and Gans, 1989; Speed et al., 1988).

Farther to the hinterland, the Central Nevada thrust belt accommodated ~10 km of shorten-ing, and it deforms rocks as deep as Lower Cambrian. At 39°N, Central Nevada thrust belt deformation consisted of growth of the Eureka culmination, a fault-bend fold that formed above a Cambrian to Silurian footwall ramp of the Ratto Canyon thrust, which is interpreted as the basal structure (Long et al., 2014). The Aptian Newark Canyon Formation was depos-ited and folded in a piggyback basin that devel-oped on the eastern limb of the Eureka culmina-tion as it grew (Long et al., 2014). To the east in the White Pine Range, stratigraphic levels from Cambrian to Pennsylvanian are exposed, without any mapped décollement horizons or thrust faults. Therefore, the Duckwater thrust is interpreted as the deformation front for the Central Nevada thrust belt at this latitude, where slip from the Ratto Canyon thrust was fed to the surface (Fig. 7). West of the Eureka culmi-nation, the geometry and stratigraphic level of the basal Central Nevada thrust belt décolle-ment are unknown, but must lie within Lower Cambrian or deeper rocks, and may eventually merge at depth with the Eastern Nevada fold belt décollement.

Deformation Timing in the Sevier Thrust Belt and Hinterland Structural Provinces

The timing of initiation of deformation in the Sevier thrust belt has been long debated; most workers agree that initial Early Cretaceous (ca. 130–125 Ma; Barremian) subsidence in the Sevier foreland basin indicates coeval crustal thickening in the thrust belt (e.g., Jordan, 1981; Lawton, 1985; DeCelles and Currie, 1996;

Long


0

-1010

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10

Approx. elevation (km)

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its:

Butte Mts.

Egan Range

Schell Creek R.

Confusion R.

House R.

White Pine R.

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igs.

5 a

nd 6

). T

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of

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ange

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ata

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ces:

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960;

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phre

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ng,

1960

; W

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1967

; D

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1967

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1974

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and

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976;

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, 197

8; B

entz

, 198

3; G

ans

and

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g et

al.,

201

2; G

reen

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014)

. The

thi

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ows

the

uppe

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it o

f Lat

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p-to

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t sim

ple

shea

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bric

s in

eas

tern

mos

t Nev

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app

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mat

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om M

iller

and

Gan

s (1

989)

. Abb

revi

atio

ns:

RM

A—

Rob

erts

Mou

ntai

ns a

lloch

thon

; C

NT

B—

Cen

tral

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a fo

ld b

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W

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—U

tah.



Lawton et al., 1997; Currie, 2002). However, on the basis of thermochronology data (Burtner and Nigrini, 1994; Ketcham et al., 1996; Yonkee et al., 1997; Stockli et al., 2001), initiation of slip on the Canyon Range thrust has been argued to be as old as the Jurassic-Cretaceous bound-ary (ca. 145 Ma; DeCelles, 2004; DeCelles and Coogan, 2006). Deformation in the Sevier thrust belt at this latitude continued through the Late Cretaceous and Paleocene (Lawton and Trexler, 1991; Lawton et al., 1993, 1997; DeCelles et al., 1995; DeCelles and Coogan, 2006), on the basis of geochronology, biostratigraphy, and struc-tural relationships of foreland basin strata.

In the Sevier hinterland, precise timing con-straints on deformation are rare, due to sparse preservation and poor geochronology of syn-orogenic rocks. Thrust faults and folds of the Western Utah thrust belt deform rocks as young as Lower Triassic, providing a maximum age bound. However, the Western Utah thrust belt diverges off of the Sevier thrust belt (Figs. 5 and 6), and on this basis, has been interpreted to be contemporary with the Cretaceous–Paleocene Sevier shortening history (Greene, 2014).

The Central Nevada thrust belt connects southward with the interior part of the Sevier thrust belt in southern Nevada (Figs. 5 and 6), which also implies an overlap in deformation timing (Taylor et al., 2000; Long, 2012). South of the Eureka culmination, rocks as young as Pennsylvanian and Permian are cut and folded by Central Nevada thrust belt structures, and in three places, undated rocks mapped as the Early Cretaceous Newark Canyon Formation are interpreted to either overlap or be cut by Central Nevada thrust belt structures (Tables 1 and 2; McDonald, 1989; Carpenter et al., 1993; Perry and Dixon, 1993). In three places, plutons rang-ing between ca. 86 Ma and ca. 108 Ma crosscut Central Nevada thrust belt structures (Table 1; McDonald, 1989; Taylor et al., 2000), indicat-ing that deformation in the southern Central Nevada thrust belt was completed by the Late Cretaceous (Albian–Coniacian). In the northern Central Nevada thrust belt, growth of the Eureka culmination is interpreted to have been contem-porary with deposition and folding of the Aptian (ca. 122–116 Ma) Newark Canyon Formation (Long et al., 2014).

First-order folds of the Eastern Nevada fold belt deform Lower Triassic rocks in multi ple places, and in one locality deform Lower Juras-sic rocks (Table 1). In addition, the Pinto Creek syncline folds the Aptian (ca. 122–116 Ma) Newark Canyon Formation in the southern Dia-mond Mountains, and it folds undated rocks mapped as the Newark Canyon Formation far-ther north in the range (Plate 1). It is suggested here that this fold province, which is defi ned

by a uniform deformation style consistent with growth of regional-scale folds above an areally extensive décollement, must have been either contemporary with or postdated the Early Creta-ceous (ca. 145–125 Ma) initial migration of the master Sevier décollement into Utah, and that construction of the Eastern Nevada fold belt as an integrated tectonic province could potentially span the Cretaceous–Paleocene deformation history recorded in the frontal Sevier thrust belt.

In summary, the Central Nevada thrust belt, Eastern Nevada fold belt, and Western Utah thrust belt represent structural provinces of the Sevier hinterland that collectively record low-magnitude (a few tens of kilometers) shorten-ing, accommodated during the protracted Cre-taceous to Paleocene detachment and eastward translation of the entire Cordilleran passive-margin basin over 220 km eastward during Sevier orogenesis. One of the principal controls on the structural style of the Sevier event was the great thickness and rheological competence of the basin through which deformation propa-gated, in particular the >6-km-thick section of Neoproterozoic–Lower Cambrian clastic rocks at its base (e.g., Armstrong, 1968, 1972; Gans and Miller, 1983; Speed et al., 1988; DeCelles, 2004). The high strength and along- and across-strike uniformity of this mechanical stratigraphy allowed Cordilleran deformation to be trans-lated eastward through a >200-km-wide hinter-land region that only experienced low-magni-tude (tens of kilometers) internal deformation. The thinning of this basin by nearly an order of magnitude eastward across the narrowly defi ned Wasatch hinge line in western Utah (e.g., Poole et al., 1992) focused the majority of Cordilleran shortening into the spatially narrow Sevier thrust belt to the east (e.g., Royse, 1993b; DeCelles, 2004). This illustrates the profound role that inherited basin geometry can exert on the loca-tion, geometry, and style of later orogenesis.

ACKNOWLEDGMENTS

S. Long is grateful to Associate Editor M.L. Wil-liams and two anonymous reviewers, whose com-ments greatly improved this manuscript.

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