Post on 11-Oct-2020
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: splong@unr.edu.
For permission to copy, contact editing@geosociety.org© 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
406 Geosphere, April 2015
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
A fold province in the Sevier hinterland in eastern Nevada
Geosphere, April 2015 407
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
408 Geosphere, April 2015
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.
A fold province in the Sevier hinterland in eastern Nevada
Geosphere, April 2015 409
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
410 Geosphere, April 2015
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.
A fold province in the Sevier hinterland in eastern Nevada
Geosphere, April 2015 411
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
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er J
uras
sic
rock
s§§§
unkn
own
unkn
own
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tern
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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
.R
eniP
etihW
nrehtroN
007–052n
wonknu°03–51
tm
RT
dloft
mR
Tot
hrP
sniatnuoM
ettuBlartne
C(c
ontin
ued
)
Long
412 Geosphere, April 2015
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
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late
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ned
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ong
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014)
. Am
plitu
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avel
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lues
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ere
repr
esen
t pre
-ext
ensi
onal
est
imat
e fr
om L
ong
et a
l. (2
014)
.† E
rosi
on le
vels
list
ed h
ere
post
date
hig
h-th
row
(2–
5 km
) no
rmal
faul
ting
that
pre
date
s th
e P
aleo
gene
unc
onfo
rmity
(Lo
ng e
t al.,
201
4).
§ Lim
b di
p es
timat
es s
how
n he
re a
ccou
nt fo
r re
stor
atio
n of
~20
°–30
°of e
astw
ard
tiltin
g th
at a
ccom
pani
ed p
re-u
ncon
form
ity n
orm
al fa
ultin
g, a
fter
Long
et a
l. (2
014)
.# F
ield
rel
atio
nshi
ps o
f Knc
and
mod
ern
limb
dips
are
des
crib
ed in
Per
ry a
nd D
ixon
(19
93),
and
cor
resp
ond
only
to th
e pa
rt o
f the
fold
that
pre
serv
es P
rh a
nd K
nc, 1
0 km
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t of t
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wn
of D
uckw
ater
.**
Bas
ed o
n re
gion
al s
trat
igra
phic
thic
knes
s da
ta fr
om S
tew
art (
1980
), in
add
ition
to s
trat
igra
phic
thic
knes
ses
from
the
cite
d m
ap s
ourc
es.
††O
rigin
ally
des
crib
ed b
y F
renc
h (1
998)
bas
ed o
n su
bcro
p pa
ttern
s in
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lroad
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ley
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es, a
nd n
amed
her
e.§§
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imat
ed b
ased
on
ampl
itude
of f
old
mea
sure
d in
cro
ss s
ectio
ns in
cite
d so
urce
map
s, b
ecau
se o
f spa
rse
data
on
the
eros
ion
leve
l of t
he P
aleo
gene
unc
onfo
rmity
in th
e D
iam
ond
Mou
ntai
ns.
##A
ppro
xim
ated
bas
ed o
n re
trod
efor
mat
ion
of ~
15°–
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f eas
twar
d til
ting
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e D
iam
ond
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ntai
ns, b
ased
on
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of T
ertia
ry r
ocks
in th
e S
ulph
ur S
prin
g R
ange
, Bal
d M
ount
ain,
and
the
nort
h en
d of
the
Dia
mon
d M
ount
ains
.**
*Tot
al tr
acea
ble
map
leng
th e
stim
ated
from
the
subc
rop
map
of L
ong
(201
2).
††† M
ap p
atte
rn e
stim
ated
from
sub
crop
map
s in
this
stu
dy, G
ans
and
Mill
er (
1983
), a
nd L
ong
(201
2).
§§§ B
ased
on
map
ping
of r
ocks
nea
r C
urrie
, Nev
ada,
that
are
cor
rela
ted
with
the
Low
er J
uras
sic
Azt
ec s
ands
tone
of s
outh
ern
Nev
ada
(Ste
war
t and
Car
lson
, 197
8; C
oats
, 198
7).
### E
stim
ated
from
the
subc
rop
map
of G
ans
and
Mill
er (
1983
).**
**In
terp
rete
d by
Gre
ene
(201
4) a
s a
stru
ctur
al lo
w c
reat
ed b
y fo
ldin
g ab
ove
east
-ver
gent
thru
st fa
ults
. Tra
ceab
le le
ngth
from
Gre
ene
(201
4, a
nd r
efer
ence
s th
erei
n).
††††
Mea
sure
d fr
om c
ross
sec
tions
of G
reen
e (2
014)
. Am
plitu
de a
nd P
aleo
gene
ero
sion
leve
ls r
epor
ted
for
wes
tern
lim
b on
ly, b
ecau
se e
aste
rn li
mb
has
been
mod
ified
by
grow
th o
f the
Sev
ier
culm
inat
ion.
A fold province in the Sevier hinterland in eastern Nevada
Geosphere, April 2015 413
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
5
10
15
20
Freq
uenc
y
14
n = 52 35 = this study 17 = Gans and Miller (1983)14 14
42
31
0
5
10
15
20
Freq
uenc
y
4
n = 36 (this study)
12
6 7
1 24
0
5
10
15
20
25
Freq
uenc
y
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
414 Geosphere, April 2015
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
ArizonaUtah
Cal.
Uta
hN
evad
aA
rizon
aN
evad
aNevada
CedarCity
St. George
Beaver
Delta
Wendover
Ely
Wells
Elko
Carlin
Eureka
Pioche
Ogden
0 10050
kilometers
SDD
SRCC
REHCC
Area of
Plate 1
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al N
ev
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ath
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lt
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ste
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elt
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ld-
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elt
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ste
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ev
ad
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ld b
elt
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SC
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AT MPT
DT
LAS
PCS
MSS
TSA
BFS
ST
GMPTS
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BRT
DWCTS
PVTS
KCT
CSA
BWT
SMT
CNTS
SRT
SVT TVT
SRT
BCT
N
WPT
KT
GPT
CLT
SDT Sevi
er fo
ld-
thru
st b
elt
IT
CCA
PMT
Present day
LVVSZ
41°N
37°N
39°N
114°W 112°W
116°W
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.
A fold province in the Sevier hinterland in eastern Nevada
Geosphere, April 2015 415
Provo
SaltLakeCity
Delta
CedarCity
St. George
Beaver
Pioche
Eureka
Ely
Wendover
?
??
0 10050kilometers
NV UT
NV UT
Ce
ntr
al N
ev
ad
ath
rust
be
lt
We
ste
rn U
tah
thru
st b
elt
Sevie
r fo
ld-
thru
st b
elt
Ea
ste
rn N
ev
ad
afo
ld b
elt
RMT
BS
PS
CS
IA
SCEC
AT MPT
DT LAS
PCS
PTS
MSS
TSABFS
ST
GMPTS
RLFTS
BRT
DWCTS
PVTS
KCT
CSA
BWT
SMT
PXTGT
CNTS
SRT
SVT
TVT
SRT
ATCT
BCT
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
416 Geosphere, April 2015
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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ks; c
ut b
y 86
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on††
††27
00 m
§§§§
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47N
ote:
Uni
t abb
revi
atio
ns s
how
n on
par
t A o
f Pla
te 1
.*F
or e
xam
ple,
Sm
ith a
nd K
etne
r (1
968)
, Joh
nson
and
Pen
derg
ast (
1981
), B
urch
fiel a
nd R
oyde
n (1
991)
, Spe
ed a
nd S
leep
(19
82).
† Bas
ed o
n in
terp
reta
tion
of D
w a
s pa
rt o
f Rob
erts
Mou
ntai
ns a
lloch
thon
by
Ste
war
t and
Poo
le (
1974
), S
tew
art a
nd C
arls
on (
1978
), a
nd H
ose
(198
3).
§ Des
crib
ed in
Lon
g et
al.
(201
4); 2
000–
2500
m th
row
whe
re d
rille
d; 3
500
m th
row
est
imat
ed fu
rthe
r to
nor
th w
here
roc
ks a
s de
ep a
s Lo
wer
Cam
bria
n ar
e in
han
ging
wal
l.# B
ased
on
stra
tigra
phic
thic
knes
s da
ta fr
om S
tew
art (
1980
), in
add
ition
to s
trat
igra
phic
thic
knes
ses
from
the
cite
d m
ap s
ourc
es.
**N
amed
by
Car
pent
er e
t al.
(199
3, p
. 65)
, the
aut
hors
sta
te th
at th
e M
oody
Pea
k th
rust
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s K
nc; h
owev
er, t
hese
dep
osits
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bio
stra
tigra
phic
age
con
trol
.††
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108
± 3
Ma
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r bi
otite
) P
uma
Hill
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ck c
uts
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ctur
es a
ssoc
iate
d w
ith th
e P
anca
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rust
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tem
(N
olan
et a
l., 1
974;
McD
onal
d, 1
989)
.§§
McD
onal
d (1
989)
sta
tes
that
und
ated
con
glom
erat
e m
appe
d as
Knc
ove
rlaps
the
Gre
en S
prin
gs th
rust
.##
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crib
ed b
y C
arpe
nter
et a
l. (1
993)
, bas
ed o
n re
inte
rpre
tatio
n of
the
map
ping
of H
ose
and
Bla
ke (
1976
).**
*Est
imat
ed u
sing
str
atig
raph
ic th
ickn
esse
s fr
om H
umph
rey
(196
0), N
olan
et a
l. (1
974)
, and
Ste
war
t (19
80).
††† M
appe
d as
an
unna
med
thru
st fa
ult b
y Q
uinl
ivan
et a
l. (1
974)
, and
nam
ed h
ere.
Alte
rnat
ivel
y in
terp
rete
d as
a n
orm
al fa
ult b
y P
erry
and
Dix
on (
1993
).§§
§ Bas
ed o
n co
rrel
atio
n of
the
Rat
to C
anyo
n th
rust
with
the
Moo
dy P
eak
thru
st.
### S
umm
ariz
ed in
Tay
lor
et a
l. (2
000)
: cor
rela
tive
stru
ctur
es 3
0–40
km
S o
f Pla
te 1
cut
roc
ks a
s yo
ung
as P
enns
ylva
nian
, and
are
cro
sscu
t by
the
ca. 9
0–98
Ma
Linc
oln
stoc
k.**
**C
orre
spon
ds to
the
tota
l tra
ceab
le le
ngth
on
the
subc
rop
map
of L
ong
(201
2), b
ased
on
corr
elat
ions
orig
inal
ly p
ropo
sed
by T
aylo
r et
al.
(200
0).
††††
Sum
mar
ized
in T
aylo
r et
al.
(200
0): a
han
ging
-wal
l ant
iclin
e in
terp
rete
d to
be
rela
ted
to m
otio
n on
the
Sch
ofiel
d C
anyo
n th
rust
is c
ut b
y th
e 86
.4 ±
4.6
Ma
Troy
gra
nite
sto
ck.
§§§§
The
Sch
ofiel
d C
anyo
n th
rust
was
not
ero
sion
ally
bre
ache
d by
the
Pal
eoge
ne. S
trat
igra
phic
thro
w is
est
imat
ed a
t 270
0 m
by
Fry
xell
(199
1).
A fold province in the Sevier hinterland in eastern Nevada
Geosphere, April 2015 417
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
418 Geosphere, April 2015
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
A fold province in the Sevier hinterland in eastern Nevada
Geosphere, April 2015 419
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
420 Geosphere, April 2015
0
-1010
0 -10
10
Approx. elevation (km)
Se
vie
r th
rust
be
lt s
tra
tig
rap
hic
un
its:
Butte Mts.
Egan Range
Schell Creek R.
Confusion R.
House R.
White Pine R.
Pancake R.
Diamond Mts.
Fish Creek R.
Mahogany Hills
Snake R.
Neo
prot
eroz
oic-
Low
er C
ambr
ian
Pale
ozoi
cTr
iass
ic-J
uras
sic
Cret
aceo
us-T
ertia
rySi
luria
n
Dev
onia
nM
issi
ssip
pian
Penn
sylv
ania
nN
eopr
oter
ozoi
cLo
wer
Cam
bria
mM
iddl
e-U
pper
Cam
bria
nO
rdov
icia
nO
rdov
icia
n (R
MA
)Pe
rmia
nTr
iass
icLo
wer
Cre
tace
ous
Prec
ambr
ian
Prec
ambr
ian
Se
vie
r h
inte
rla
nd
str
ati
gra
ph
ic u
nit
s:Cany
on R
ange
thru
stPa
vant
thru
stPa
xton
thru
stG
unni
son
thru
stSe
vier
culm
inat
ion
mod
ified
from
DeC
elle
san
d Co
ogan
(200
6)m
odifi
ed fr
omG
reen
e (2
014)
mod
ified
from
Long
et a
l. (2
014)
Se
vie
r fo
ld-t
hru
st b
elt
We
ste
rn U
tah
th
rust
be
ltE
ast
ern
Ne
va
da
fo
ld b
elt
Ce
ntr
al
Ne
va
da
th
rust
be
lt
Conf
usio
nsy
nclin
oriu
mBu
tte
sync
linor
ium
Illip
ahan
ticlin
e
Eure
kacu
lmin
atio
n
Knc
pigg
ybac
kba
sin
Ratt
o Ca
nyon
thru
st
Robe
rts
Mts
.th
rust
Duc
kwat
erth
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??
1
010
20
kilo
met
ers
NV
UT
?
Pale
ogen
eun
conf
orm
ity
24
35
6
East
Wes
t
Mor
itz-
Nag
erth
rust
Fo
otn
ote
s:
1 - b
asal
Sev
ier d
ecol
lem
ent o
f DeC
elle
s an
d Co
ogan
(200
6)2
- hig
hest
pos
sibl
e le
vel o
f Can
yon
Rang
e th
rust
3 - b
asal
WU
TB d
efor
mat
ion
leve
l mus
t dee
pen
rapi
dly
tow
ard
wes
t4
- hig
hest
pos
sibl
e le
vel o
f WU
TB a
nd E
NFB
dec
olle
men
t5
- CN
TB d
efor
mat
ion
is in
terp
rete
d to
day
light
at D
uckw
ater
thru
st b
ecau
se th
rust
faul
ts a
re n
ot o
bser
ved
at a
ny le
vel o
f Cam
bria
n-Pe
nnsy
lvan
ian
expo
sure
in W
hite
Pin
e Ra
nge
6 - l
evel
of C
NTB
dec
olle
men
t is
unkn
own
wes
t of E
urek
a cu
lmin
atio
n
?
uppe
r lim
it of
top-
to-e
ast
sim
ple
shea
r (~7
0-90
Ma)
Fig
ure
7. G
ener
aliz
ed c
ross
-sec
tion
thro
ugh
east
ern
Nev
ada
and
wes
tern
Uta
h at
~39°N
, sho
win
g th
e ge
omet
ry o
f the
Sev
ier
fold
-and
-thr
ust
belt
(m
odifi
ed f
rom
DeC
elle
s an
d C
ooga
n, 2
006,
the
ir F
ig. 8
F),
and
str
uctu
ral
prov
ince
s of
the
Sev
ier
hint
erla
nd. T
his
is n
ot a
bal
ance
d cr
oss
sect
ion;
it is
mea
nt t
o ill
ustr
ate
appr
oxim
ate
defo
rmat
ion
geom
etri
es a
nd c
onst
rain
ts o
n dé
colle
men
t le
vels
in t
he S
evie
r hi
nter
land
. T
he h
inte
rlan
d po
rtio
n is
dra
fted
bas
ed o
n ho
rizo
ntal
dis
tanc
es o
n th
e 36
Ma
tect
onic
rec
onst
ruct
ion
of M
cQua
rrie
and
Wer
nick
e (2
005)
sh
own
on F
igur
e 6,
and
it u
ses
stra
tigr
aphi
c th
ickn
ess
data
fro
m S
tew
art
(198
0), G
ans
and
Mill
er (
1983
), G
reen
e (2
014)
, and
Lon
g et
al.
(201
4). T
he P
aleo
gene
unc
onfo
rmit
y is
dra
wn
as a
hor
izon
tal d
atum
, at a
n ap
prox
imat
e el
evat
ion
of 2
.5 k
m, a
fter
Sne
ll et
al.
(201
4), a
nd it
s st
rati
grap
hic
leve
ls fr
om P
late
1 a
nd L
ong
(201
2) w
ere
used
to c
onst
rain
app
roxi
mat
e ge
omet
ries
for
fi rst
-ord
er fo
lds
of th
e E
aste
rn N
evad
a fo
ld b
elt
(not
e th
at t
he s
peci
fi c f
orm
atio
n m
echa
nism
at
dept
h fo
r th
ese
fold
s is
not
inte
rpre
ted
on t
he c
ross
sec
tion
, and
tha
t th
is t
rans
ect
does
not
con
tain
all
of t
he fi
rst
-ord
er f
olds
of
the
Eas
tern
Nev
ada
fold
bel
t; s
ee F
igs.
5 a
nd 6
). T
rans
luce
nt a
reas
abo
ve t
he P
aleo
gene
un
conf
orm
ity
repr
esen
t er
oded
roc
k. T
hick
gre
en li
nes
show
the
tot
al r
ange
of
stra
tigr
aphi
c le
vels
pre
sent
ly e
xpos
ed in
indi
vidu
al r
ange
s (d
ata
sour
ces:
Dou
glas
s, 1
960;
Hum
phre
y, 1
960;
You
ng,
1960
; W
oodw
ard,
196
2; B
roka
w,
1967
; D
eche
rt,
1967
; N
olan
et
al.,
1974
; H
ose
and
Bla
ke, 1
976;
Sch
alla
, 197
8; B
entz
, 198
3; G
ans
and
Mill
er, 1
983;
Ott
o, 2
008;
Lon
g et
al.,
201
2; G
reen
e, 2
014)
. The
thi
ck, d
ashe
d re
d lin
e sh
ows
the
uppe
r lim
it o
f Lat
e C
reta
ceou
s, to
p-to
-eas
t sim
ple
shea
r fa
bric
s in
eas
tern
mos
t Nev
ada,
app
roxi
mat
ed fr
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
Nev
ada
thru
st b
elt;
EN
FB
—E
aste
rn N
evad
a fo
ld b
elt;
W
UT
B—
Wes
tern
Uta
h th
rust
bel
t; N
V—
Nev
ada;
UT
—U
tah.
A fold province in the Sevier hinterland in eastern Nevada
Geosphere, April 2015 421
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.
REFERENCES CITED
Allmendinger, R.W., 1992, Fold and thrust tectonics of the western United States exclusive of the accreted terranes, in Burchfi el, B.C., Lipman, P.W., and Zoback, M.L., eds., The Cordilleran Orogen: Conterminous U.S.: Boulder, Colorado, Geological Society of America, The Geology of North America, v. G-3, p. 583–607.
Allmendinger, R.W., Sharp, J.W., Von Tish, D., Serpa, L., Brown, L., Kaufman, S., and Oliver, J., 1983, Cenozoic and Mesozoic structure of the eastern Basin and Range Province, Utah, from COCORP seismic-reflection data: Geology, v. 11, p. 532–536, doi: 10 .1130 /0091 -7613 (1983)11 <532: CAMSOT>2 .0 .CO;2 .
Allmendinger, R.W., Farmer, H., Hauser, E., Sharp, J., Von Tish, D., Oliver, J., and Kaufman, S., 1986, Phanero-zoic tectonics of the Basin and Range–Colorado Pla-teau transition from COCORP data and geologic data:
A review: American Geophysical Union Geodynamic Monograph 14, p. 257–267.
Allmendinger, R.W., Hauge, T., Hauser, E.C., Potter, C.J., Klemperer, S.L., Nelson, D.K., Knuepfer, P., and Oli-ver, J., 1987, Overview of the COCORP 40°N tran-sect, western United States; the fabric of an orogenic belt: Geological Society of America Bulletin, v. 98, p. 308–319, doi: 10 .1130 /0016 -7606 (1987)98 <308: OOTCNT>2 .0 .CO;2 .
Armstrong, R.L., 1968, Sevier orogenic belt in Nevada and Utah: Geological Society of America Bulletin, v. 79, p. 429–458, doi: 10 .1130 /0016 -7606 (1968)79 [429: SOBINA]2 .0 .CO;2 .
Armstrong, R.L., 1972, Low-angle (denudation) faults, hinter land of the Sevier orogenic belt, eastern Nevada and western Utah: Geological Society of America Bul-letin, v. 83, p. 1729–1754, doi: 10 .1130 /0016 -7606 (1972)83 [1729: LDFHOT]2 .0 .CO;2 .
Armstrong, R.L., and Ward, P., 1991, Evolving geographic patterns of Cenozoic magmatism in the North Ameri-can Cordillera: The temporal and spatial association of magmatism and metamorphic core complexes: Journal of Geophysical Research, v. 96, p. 13,201–13,224, doi: 10 .1029 /91JB00412 .
Bartley, J.M., and Gleason, G.C., 1990, Tertiary normal faults superimposed on Mesozoic thrusts, Quinn Canyon and Grant Ranges, Nye County, Nevada, in Wernicke , B.P., ed., Basin and Range Extensional Tec-tonics Near the Latitude of Las Vegas, Nevada: Geo-logical Society of America Memoir 176, p. 195–212.
Bentz, M.G., 1983, Progressive Structural and Stratigraphic Events Affecting the Roberts Mountains Alloch-thon in the Devil’s Gate Area, Nevada [M.S. thesis]: Athens , Ohio, Ohio University, 222 p., 3 plates, 1:9600 scale map.
Best, M.G., and Christiansen, E.H., 1991, Limited extension during peak Tertiary volcanism, Great Basin of Nevada and Utah: Journal of Geophysical Research, v. 96, p. 13,509–13,528, doi: 10 .1029 /91JB00244 .
Best, M.G., Barr, D.L., Christiansen, E.H., Gromme, S., Deino, A.L., and Tingey, D.G., 2009, The Great Basin Altiplano during the middle Cenozoic ignimbrite fl areup: Insights from volcanic rocks: International Geology Review, v. 51, p. 589–633, doi: 10 .1080 /00206810902867690 .
Brokaw, A.L., 1967, Geologic Map and Sections of the Ely Quadrangle, White Pine County, Nevada: U.S. Geo-logi cal Survey Geologic Quadrangle Map GQ-697, scale 1:24,000, 1 plate.
Brokaw, A.L., and Barosh, P.J., 1968, Geologic Map of the Riepetown Quadrangle, White Pine County, Nevada: U.S. Geological Survey Geologic Quadrangle Map GQ-758, scale 1:24,000, 1 plate.
Brokaw, A.L., and Heidrick, T., 1966, Geologic Map and Sections of the Giroux Wash Quadrangle, White Pine County, Nevada: U.S. Geological Survey Geologic Quadrangle Map GQ-476, scale 1:24,000, 1 plate.
Burchfi el, B.C., and Royden, L.H., 1991, Antler orogeny: A Mediterranean-type orogeny: Geology, v. 19, p. 66–69, doi: 10 .1130 /0091 -7613 (1991)019 <0066: AOAMTO>2 .3 .CO;2 .
Burchfi el, B.C., Cowan, D.S., and Davis, G.A., 1992, Tec-tonic overview of the Cordilleran orogen in the western United States, in Burchfi el, B.C., Lipman, P.W., and Zoback, M.L., eds., The Cordilleran Orogen: Conter-minous U.S.: Boulder, Colorado, Geological Society of America, The Geology of North America, v. G-3, p. 407–480.
Burtner, R.L., and Nigrini, A., 1994, Thermochronology of the Idaho-Wyoming thrust belt during the Sevier orog-eny: A new, calibrated, multiprocess thermal model: American Association of Petroleum Geologists Bul-letin, v. 78, p. 1568–1612.
Camilleri, P.A., 2013, Geologic Map and Structure of the West-Central Part of the Grant Range, Nye County, Nevada: Geological Society of America Digital Map and Chart Series 14, 1 sheet, 25 p., doi: 10 .1130 /2013 .DMCH014 .
Camilleri, P.A., and Chamberlain, K.R., 1997, Mesozoic tectonics and metamorphism in the Pequop Mountains and Wood Hills region, northeast Nevada: Implications for the architecture and evolution of the Sevier oro-
Long
422 Geosphere, April 2015
gen: Geological Society of America Bulletin, v. 109, p. 74–94, doi: 10 .1130 /0016 -7606 (1997)109 <0074: MTAMIT>2 .3 .CO;2 .
Camilleri, P., Yonkee, A., Coogan, J., DeCelles, P., McGrew, A., and Wells, M., 1997, Hinterland to foreland tran-sect through the Sevier orogen, northeast Nevada to north-central Utah: Structural style, metamorphism, and kinematic history of a large contractional oro-genic wedge, in Link, P.K., and Kowallis, B.J., eds., Proterozoic to Recent Stratigraphy, Tectonics, and Vol-canology, Utah, Nevada, Southern Idaho, and Central Mexico: Brigham Young University Geology Studies, v. 42, part 1, p. 297–309.
Campbell, M.D., 1981, Geology of the Northern Buck Mountain Area, White Pine County, Nevada [M.S. thesis ]: Athens, Ohio, Ohio University, 70 p.
Carlisle, D., and Nelson, C.A., 1990, Geologic Map of the Mineral Hill Quadrangle, Nevada: Nevada Bureau of Mines and Geology Map 97, 1 sheet, scale 1:48,000.
Carpenter, D.G., Carpenter, J.A., Dobbs, S.W., and Stuart, C.K., 1993, Regional structural synthesis of Eureka fold-and-thrust belt, east-central Nevada, in Gillespie, C.W., ed., Structural and Stratigraphic Relationships of Devonian Reservoir Rocks, East-Central Nevada: Reno, Nevada Petroleum Society, 1993 Field Confer-ence Guidebook, p. 59–72.
Coats, R.R., 1987, Geology of Elko County, Nevada: Nevada Bureau of Mines and Geology Bulletin 101, 112 p.
Coleman, D.S., and Glazner, A.F., 1998, The Sierra Crest magmatic event: Rapid formation of juvenile crust during the Late Cretaceous in California, in Ernst, W.G., and Nelson, C.A., eds., Integrated Earth and Environmental Evolution of the Southwestern United States: Columbia, Maryland, Bellwether Publishing, p. 253–272.
Colgan, J.P., and Henry, C.D., 2009, Rapid middle Miocene collapse of the Mesozoic orogenic plateau in north-central Nevada: International Geology Review, v. 51, p. 920–961, doi: 10 .1080 /00206810903056731 .
Colgan, J.P., Howard, K.A., Fleck, R.J., and Wooden, J.L., 2010, Rapid middle Miocene extension and unroofi ng of the southern Ruby Mountains, Nevada: Tectonics, v. 29, doi: 10 .1029 /2009TC002655 .
Collinson, J.W., and Hasenmueller, W.A., 1978, Early Triassic paleogeography and biostratigraphy of the Cordi lleran miogeocline, in Howell, D.G., and McDougall, K.A., eds., Mesozoic Paleontology of the Western United States: Los Angeles, Society of Economic Paleon-tologists and Mineralogists, Pacifi c Section, Pacifi c Coast Paleogeography Symposium 2, p. 175–187.
Colman-Sadd, S.P., 1978, Fold development in Zagros sim-ply folded belt, southwest Iran: American Association of Petroleum Geologists Bulletin, v. 62, p. 984–1003.
Coney, P.J., and Harms, T.J., 1984, Cordilleran metamorphic core complexes: Cenozoic extensional relics of Meso-zoic compression: Geology, v. 12, p. 550–554, doi: 10 .1130 /0091 -7613 (1984)12 <550: CMCCCE>2 .0 .CO;2 .
Connell, L.E., 1984, The Geology of the Northern Butte Mountains, White Pine County, Nevada [M.S. thesis] Reno, Nevada, University of Nevada, 191 p.
Cowell, P.F., 1986, Structure and Stratigraphy of Part of the Northern Fish Creek Range, Eureka County, Nevada [M.S. thesis]: Corvallis, Oregon, Oregon State Univer-sity, 96 p.
Currie, B.S., 2002, Structural confi guration of the Early Cre-taceous Cordilleran foreland-basin system and Sevier thrust belt, Utah and Colorado: The Journal of Geol-ogy, v. 110, p. 697–718, doi: 10 .1086 /342626 .
DeCelles, P.G., 1994, Late Cretaceous–Paleocene syn-orogenic sedimentation and kinematic history of the Sevier thrust belt, northeast Utah and southwest Wyo-ming: Geological Society of America Bulletin, v. 106, p. 32–56, doi: 10 .1130 /0016 -7606 (1994)106 <0032: LCPSSA>2 .3 .CO;2 .
DeCelles, P.G., 2004, Late Jurassic to Eocene evolution of the Cordilleran thrust belt and foreland basin system, western U.S.A.: American Journal of Science, v. 304, p. 105–168, doi: 10 .2475 /ajs .304 .2 .105 .
DeCelles, P.G., and Coogan, J.C., 2006, Regional structure and kinematic history of the Sevier fold-and-thrust belt, central Utah: Geological Society of America Bul-letin, v. 118, p. 841–864, doi: 10 .1130 /B25759 .1 .
DeCelles, P.G., and Currie, B.S., 1996, Long-term sediment accumulation in the Middle Jurassic–early Eocene Cordilleran retroarc foreland basin system: Geology, v. 24, p. 591–594, doi: 10 .1130 /0091 -7613 (1996)024 <0591: LTSAIT>2 .3 .CO;2 .
DeCelles, P.G., Lawton, T.F., and Mitra, G., 1995, Thrust timing, growth of structural culminations, and synoro-genic sedimentation in the type area of the Sevier oro-genic belt, central Utah: Geology, v. 23, p. 699–702, doi: 10 .1130 /0091 -7613 (1995)023 <0699: TTGOSC>2 .3 .CO;2 .
Dechert, C.P., 1967, Bedrock Geology of the Northern Schell Creek Range, White Pine County, Nevada [Ph.D. dis-sertation]: Seattle, Washington, University of Washing-ton, 304 p.
Dickinson, W.R., 2000, Geodynamic interpretation of Paleo-zoic tectonic trends oriented oblique to the Mesozoic Klamath-Sierran continental margin in California, in Soreghan, M.J., and Gehrels, G.E., eds., Paleozoic and Triassic Paleogeography and Tectonics of Western Nevada and Northern California: Geological Society of America Special Paper 347, p. 209–245.
Dickinson, W.R., 2002, The Basin and Range Province as a composite extensional domain: International Geology Review, v. 44, p. 1–38, doi: 10 .2747 /0020 -6814 .44 .1 .1 .
Dickinson, W.R., 2004, Evolution of the North American Cordillera: Annual Review of Earth and Planetary Sci-ences, v. 32, p. 13–45, doi: 10 .1146 /annurev .earth .32 .101802 .120257 .
Dilek, Y., and Moores, E.M., 1999, A Tibetan model for the Early Tertiary western United States: Journal of the Geological Society of London, v. 156, p. 929–941, doi: 10 .1144 /gsjgs .156 .5 .0929 .
Dixon, G.L., Hedlund, D.C., and Ekren, E.B., 1972, Geo-logic Map of the Pritchards Station Quadrangle, Nye County, Nevada: U.S. Geological Survey Miscel-laneous Geologic Investigations Map I-728, scale 1:48,000, 1 plate.
Douglass, W.B., Jr., 1960, Geology of the southern Butte Mountains, White Pine County, Nevada, in Boettcher, J.W., and Sloan, W.W., Jr., eds., Guidebook to the Geology of East-Central Nevada: Salt Lake City, Utah, Intermountain Association of Petroleum Geologists, 11th Annual Field Conference, p. 181–185.
Drake, E.A., 1978, Paleozoic Stratigraphy of the Devil’s Gate–Northern Mahogany Hills Area, Eureka County, Nevada [M.S. thesis]: Reno, University of Nevada, 110 p., 6 plates, scale 1:24,000 map.
Druschke, P., Hanson, A.D., and Wells, M.L., 2009a, Struc-tural, stratigraphic, and geochronologic evidence for extension predating Paleogene volcanism in the Sevier hinterland, east-central Nevada: International Geology Review, v. 51, p. 743–775, doi: 10 .1080 /00206810902917941 .
Druschke, P., Hanson, A.D., Wells, M.L., Rasbury, T., Stockli, D.F., and Gehrels, G., 2009b, Synconvergent surface-breaking normal faults of Late Cretaceous age within the Sevier hinterland, east-central Nevada: Geology, v. 37, p. 447–450, doi: 10 .1130 /G25546A .1 .
Druschke, P., Hanson, A.D., Wells, M.L., Gehrels, G.E., and Stockli, D., 2010, Paleogeographic isolation of the Cretaceous to Eocene Sevier hinterland, east-central Nevada: Insights from U-Pb and (U-Th)/He detrital zircon ages of hinterland strata: Geological Society of America Bulletin, v. 123, p. 1141–1160, doi: 10 .1130 /B30029 .1 .
duBray, E.A., and Hurtubise, D.O., 1994, Geologic Map of the Seaman Range, Lincoln and Nye Counties, Nevada: U.S. Geological Survey Miscellaneous Inves-tigations Series Map I- 2282, scale 1:50,000.
Ducea, M., 2001, The California arc: Thick granitic batho-liths, eclogitic residues, lithospheric-scale thrusting, and magmatic fl are-ups: GSA Today, v. 11, p. 4–10, doi: 10 .1130 /1052 -5173 (2001)011 <0004: TCATGB>2 .0 .CO;2 .
Ekren, E.B., Hinrichs, E.N., and Dixon, G.L., 1972, Geo-logic Map of the Wall Quadrangle, Nye County, Nevada: U.S. Geological Survey Miscellaneous Geo-logic Investigations Map I-719, scale 1:48,000, 1 plate.
Ekren, E.B., Hinrichs, E.N., Quinlivan, W.D., and Hoover, D.L., 1973a, Geologic Map of the Moores Station Quadrangle, Nye County, Nevada: U.S. Geological
Survey Miscellaneous Geologic Investigations Map I-756, scale 1:48,000, 1 plate.
Ekren, E.B., Rogers, C.L., and Dixon, G.L., 1973b, Geo-logic and Bouguer Gravity Map of the Reveille Quad-rangle, Nye County, Nevada: U.S. Geological Survey Miscellaneous Investigations Series Map I-806, scale 1:48,000, 1 plate.
Ekren, E.B., Rowley, P.D., Dixon, G.L., Page, W.R., Klein-hampl, F.J., Ziony, J.I., Brandt, J.M.,, and Patrick, B.G., 2012, Geology of the Quinn Canyon Range and Vicinity, Nye and Lincoln Counties, Nevada: South-ern Nevada Water Authority, Groundwater Resources Department, Water Resources Division, Document Number HAM-ED-0004, 60 p., 1 plate, scale 1:100,000.
Epard, J.L., and Groshong, R.H., Jr., 1993, Excess area and depth to detachment: American Association of Petro-leum Geologists Bulletin, v. 77, p. 1291–1302.
Faill, R.T., 1998, A geologic history of the north-central Appalachians: Part 3. The Alleghany orogeny: Ameri-can Journal of Science, v. 298, p. 131–179, doi: 10 .2475 /ajs .298 .2 .131 .
Feeley, T.C., 1993, Geologic Map of the Robinson Summit Quadrangle, Nevada: Nevada Bureau of Mines and Geology Field Studies Map 2, scale 1:24,000, 1 plate.
Fouch, T.D., Hanley, J.M., and Forester, R.M., 1979, Prelimi-nary correlation of Cretaceous and Paleogene lacustrine and related nonmarine sedimentary and volcanic rocks in parts of the Great Basin of Nevada and Utah, in New-man, G.W., and Goode, H.D., eds., Basin and Range Symposium and Great Basin Field Conference: Denver, Rocky Mountain Association of Petroleum Geologists and Utah Geological Association, p. 305–312.
Fouch, T.D., Lund, K., Schmitt, J.G., Good, S.C., and Hanley , J.H., 1991, Late Cretaceous(?) and Paleogene sedimen-tary rocks and extensional(?) basins in the region of the Egan and Grant Ranges, and White River and Railroad Valleys, Nevada: Their relation to Sevier and Laramide contractional basins in the southern Rocky Mountains and Colorado Plateau, in Flanigan, D.M.H., Hansen, M., and Flanigan, T.E., eds., Geology of the White River Valley, the Grant Range, Eastern Railroad Valley and the Western Egan Range, Nevada: Nevada Petro-leum Society 1991 Fieldtrip Guidebook: Reno, Nevada, Nevada Petroleum Society, p. 15–23.
French, D.E., 1993, Thrust faults in the southern Diamond Mountains, Eureka and White Pine Counties, Nevada, in Gillespie, C.W., ed., Structural and Stratigraphic Relationships of Devonian Reservoir Rocks, East-Cen-tral Nevada: Reno, Nevada, Nevada Petroleum Society, 1993 Field Conference Guidebook, p. 105–114.
French, D.E., 1998, Petroleum systems of the Great Basin: The Railroad Valley model, in French, D.E., and Schalla, R.A., eds., Hydrocarbon Habitat and Special Geologic Problems of the Great Basin: Reno, Nevada, Nevada Petroleum Society, 1998 Field Trip Guide-book, p. 38–56.
Fritz, W.H., 1968, Geologic Map and Sections of the South-ern Cherry Creek and Northern Egan Ranges, White Pine County, Nevada: Nevada Bureau of Mines and Geology Map 35, scale 1:62,500, 1 plate.
Fryxell, J.E., 1988, Geologic Map and Description of Stratigraphy and Structure of the West-Central Grant Range, Nye County, Nevada: Geological Society of America Map and Chart Series MCH064, 16 p., 2 sheets, scale 1:24,000.
Fryxell, J.E., 1991, Tertiary tectonic denudation of an igne-ous and metamorphic complex, west-central Grant Range, Nye County, Nevada, in Raines, G.L., et al., eds., Geology and Ore Deposits of the Great Basin: Symposium and Proceedings: Reno, Nevada, Geologi-cal Society of Nevada, p. 87–92.
Gans, P.B., and Miller, E.L., 1983, Style of mid-Tertiary extension in east-central Nevada: Utah Geological and Mineral Survey Special Studies, v. 59, p. 107–160.
Greene, D.C., 2014, The Confusion Range, west-central Utah: Fold-thrust deformation and a western Utah thrust belt in the Sevier hinterland: Geosphere, v. 10, p. 148–169, doi: 10 .1130 /GES00972 .1 .
Guerrero, J.A., 1983, Geology of the Northern White Pine Range, East-Central Nevada [M.S. thesis]: Long Beach, California, California State University, 105 p., 3 plates, scale 1:24,000.
A fold province in the Sevier hinterland in eastern Nevada
Geosphere, April 2015 423
Gwinn, V.E., 1970, Kinematic patterns and estimates of lateral shortening, Valley and Ridge and Great Valley Provinces, central Appalachians, south-central Penn-sylvania, in Fisher, G.W., Pettijohn, F.J., Reed, J.C., Jr., and Weaver, K.N., eds., Studies of Appalachian Geology: Central and Southern New York: New York, Interscience Publishers, p. 127–146.
Harris, H.D., 1959, A late Mesozoic positive area in western Utah: American Association of Petroleum Geologists Bulletin, v. 43, p. 2636–2652.
Haworth, W.D., 1979, Geology of the Northern Part of the Diamond Range, Eureka and White Pine Counties, Nevada [M.S. thesis]: Reno, Nevada, University of Nevada, 68 p., 3 plates, scale 1:20,000.
Heller, P.L., Bowdler, S.S., Chambers, H.P., Coogan, J.C., Hagen, E.S., Shuster, M.W., Winslow, N.S., and Law-ton, T.F., 1986, Time of initial thrusting in the Sevier orogenic belt, Idaho-Wyoming and Utah: Geology, v. 14, p. 388–391, doi: 10 .1130 /0091 -7613 (1986)14 <388: TOITIT>2 .0 .CO;2 .
Hess, R.H., Fitch, S.P., and Warren, S.N., 2004, Nevada Oil and Gas Well Database: Nevada Bureau of Mines and Geology Open-File Report 04–1, 4 p.
Hintze, L.F., and Davis, F.D., 2003, Geology of Millard Country, Utah: Utah Geological Survey Bulletin 133, 305 p.
Hintze, L.F., Willis, G.C., Laes, D.Y.M., Sprinkel, D.A. and Brown, K.D., 2000, Digital Geologic Map of Utah: Utah Geological Survey Map 179DM, scale 1:500,000.
Hose, R.K., 1977, Structural Geology of the Confusion Range, West-Central Utah: U.S. Geological Survey Professional Paper 971, p. 97–131.
Hose, R.K., 1983, Geologic Map of the Cockalorum Wash Quadrangle, Eureka and Nye Counties, Nevada: U.S. Geological Survey Miscellaneous Investigations Series Map I-1410, scale 1:31,680, 1 plate.
Hose, R.K., and Blake, M.C., Jr., 1976, Geologic Map of White Pine County, Nevada: U.S. Geological Survey Open-File Report OF-70-166, scale 1:250,000.
Humphrey, F.L., 1960, Geology of the White Pine Mining District, White Pine County, Nevada: Nevada Bureau of Mines and Geology Bulletin 57, scale 1:48,000, 1 plate, 67 p.
Johnson, J.G., and Pendergast, A., 1981, Timing and mode of emplacement of the Roberts Mountains allochthon, Antler orogeny: Geological Society of America Bulle-tin, v. 92, p. 648–658, doi: 10 .1130 /0016 -7606 (1981)92 <648: TAMOEO>2 .0 .CO;2 .
Jones, C.H., Sonder, L.J., and Unruh, J.R., 1998, Litho-spheric gravitational potential energy and past oro-genesis: Implications for conditions of initial Basin and Range and Laramide deformation: Geology, v. 26, p. 639–642, doi: 10 .1130 /0091 -7613 (1998)026 <0639: LGPEAP>2 .3 .CO;2 .
Jordan, T.E., 1981, Thrust loads and foreland basin evolu-tion, Cretaceous, western United States: American Association of Petroleum Geologists Bulletin, v. 65, p. 2506–2520.
Kellogg, H.E., 1964, Cenozoic stratigraphy and structure of the southern Egan Range, Nevada: Geological Society of America Bulletin, v. 75, p. 949–968, 2 plates.
Ketcham, R.A., Donelick, R.A., Linn, J.K., and Walker, J.D., 1996, Effects of kinetic variation on interpretation and modeling of apatite fi ssion track data; application to central Utah: Geological Society of America Abstracts with Programs, v. 28, no. 7, p. 441.
Kleinhampl, F.J., and Ziony, J.L., 1985, Geology of North-ern Nye County, Nevada: Nevada Bureau of Mines Bulletin 99A, 171 p.
Kulander, B.R., and Dean, S.L., 1986, Structure and tec-tonics of central and southern Appalachian Valley and Ridge and Plateau Provinces, West Virginia and Vir-ginia: American Association of Petroleum Geologists Bulletin, v. 70, p. 1674–1684.
Larson, E.R., and Riva, J.F., 1963, Preliminary Geologic Map and Sections of the Diamond Springs Quadrangle: Nevada Bureau of Mines and Geology Map 20, scale 1:62,550, 1 plate.
Lawton, T.F., 1985, Style and timing of frontal structures, thrust belt, central Utah: American Association of Petroleum Geologists Bulletin, v. 69, p. 1145–1159.
Lawton, T.F., and Trexler, J.H., Jr., 1991, Piggyback basin in the Sevier thrust belt, Utah: Implications for develop-ment of the thrust wedge: Geology, v. 19, p. 827–830, doi: 10 .1130 /0091 -7613 (1991)019 <0827: PBITSO>2 .3 .CO;2 .
Lawton, T.F., Talling, P.J., Hobbs, R.S., Trexler, J.H., Jr., Weiss, M.P., and Burbank, D.W., 1993, Structure and stratigraphy of Upper Cretaceous and Paleogene strata (North Horn Formation), eastern San Pitch Mountains, Utah—Sedimentation at the front of the Sevier orogenic belt: U.S. Geological Survey Bulletin 1787, p. II1–II33.
Lawton, T.F., Sprinkel, D., DeCelles, P.G., Mitra, G., and Sussman, A.J., 1997, Thrusting and synorogenic sedi-mentation in the central Utah Sevier thrust belt and foreland basin: Brigham Young University Geology Studies, v. 42, part 2, p. 33–67.
Lipka, J.T., 1987, Stratigraphy and Structure of the Southern Sulphur Springs Range, Eureka County, Nevada [M.S. thesis]: Corvallis, Oregon, University of Oregon, 94 p., 4 plates, scale 1:24,000.
Long, S.P., 2012, Magnitudes and spatial patterns of ero-sional exhumation in the Sevier hinterland, eastern Nevada and western Utah, USA: Insights from a Paleo-gene paleogeologic map: Geosphere, v. 8, p. 881–901, doi: 10 .1130 /GES00783 .1 .
Long, S.P., Henry, C.D., Muntean, J.H., Edmondo, G.P., and Thomas, R.D., 2012, Preliminary Geologic Map of the Southern Eureka Mining District, Eureka and White Pine Counties, Nevada: Nevada Bureau of Mines and Geology Open-File Report 12–6, scale 1:24,000, 2 plates.
Long, S.P., Henry, C.D., Muntean, J.L., Edmondo, G.P., and Cassel, E.J., 2014, Early Cretaceous construction of a structural culmination, Eureka, Nevada, U.S.A.: Impli-cations for out-of-sequence deformation in the Sevier hinterland: Geosphere, v. 10, p. 564–584, doi: 10 .1130 /GES00997 .1 .
Low, D.J., 1982, Geology of Whistler Mountain, Eureka County, Nevada [M.S. thesis]: Lincoln, Nebraska, Uni-versity of Nebraska, 127 p., 4 plates, scale 1:62,500.
Lund, K., Nash, J.T., Beard, L.S., Blank, H.R., Jr., and Tuftin, S.E., 1987, Mineral Resources of the Blue Eagle Wilderness Study Area, Nye County, Nevada: U.S. Geological Survey Bulletin 1731-D, 19 p.
Lund, K., Beard, L.S., Blank, H.R., Jr., Hofstra, A.H., and Hamilton, M.M., 1988, Mineral Resources of the Rior-dans Well Wilderness Study Area, Nye County, Nevada: U.S. Geological Survey Bulletin 1731-H, 16 p.
Martin, M.W., and Naumann, T.R., 1995, Geological Map of the Reveille Quadrangle, Nevada: Nevada Bureau of Mines and Geology Map 104, scale 1:24,000, 1 plate, 6 p.
McDonald, S.F., 1989, Geology, Pogues Station Quad-rangle, White Pine and Nye Counties, Nevada [M.S. thesis]: San Diego, California, San Diego State Uni-versity, 107 p.
McGrew, A.J., Peters, M.T., and Wright, J.E., 2000, Thermo-barometric constraints on the tectonothermal evolution of the East Humboldt Range metamorphic core com-plex, Nevada: Geological Society of America Bulletin, v. 112, p. 45–60, doi: 10 .1130 /0016 -7606 (2000)112 <45: TCOTTE>2 .0 .CO;2 .
McKee, E.H., and Conrad, J.E., 1998, Geologic Map of the Frazier Creek Quadrangle, Nevada: Nevada Bureau of Mines and Geology Field Studies Map 15, scale 1:24,000, 1 sheet.
McQuarrie, N., 2004, Crustal-scale geometry of the Zagros fold-thrust belt, Iran: Journal of Structural Geology, v. 26, p. 519–535, doi: 10 .1016 /j .jsg .2003 .08 .009 .
McQuarrie, N., and Wernicke, B.P., 2005, An animated tec-tonic reconstruction of southwestern North America since 36 Ma: Geosphere, v. 1, p. 147–172, doi: 10 .1130 /GES00016 .1 .
Miller, D.M., and Hoisch, T.D., 1995, Jurassic tectonics of northeastern Nevada and northwestern Utah from the perspective of barometric studies, in Miller, D.M., and Busby, C., eds., Jurassic Magmatism and Tectonics of the North American Cordillera: Geological Society of America Special Paper 299, p. 267–294, doi: 10 .1130 /SPE299 -p267 .
Miller, E.L., and Gans, P.B., 1989, Cretaceous crustal struc-ture and metamorphism in the hinterland of the Sevier
thrust belt, western U.S. Cordillera: Geology, v. 17, p. 59–62, doi: 10 .1130 /0091 -7613 (1989)017 <0059: CCSAMI>2 .3 .CO;2 .
Miller, E.L., Gans, P.B., Wright, J.E., and Sutter, J.F., 1988, Metamorphic history of the east-central Basin and Range Province: Tectonic setting and relationship to magmatism, in Ernst, W.G., ed., Metamorphism and Crustal Evolution, Western Conterminous United States, Rubey Volume 7: Englewood Cliffs, New Jer-sey, Prentice-Hall, p. 649–682.
Miller, E.L., Miller, M.M., Stevens, C.H., Wright, J.E., and Madrid, R., 1992, Late Paleozoic paleogeographic and tectonic evolution of the western U.S. Cordillera, in Burchfi el, B.C., Lipman, P.W., and Zoback, M.L., eds., The Cordilleran Orogen: Conterminous U.S.: Boulder, Colorado, Geological Society of America, The Geol-ogy of North America, v. G-3, p. 57–106.
Millikan, G.R., 1979, Geology of a Portion of the Sher-man Mountain Quadrangle, Nevada [M.S. thesis]: San Diego, California, San Diego State University, 79 p., 2 plates, scale 1:31,250.
Mitra, G., 1997, Evolution of salients in a fold-and-thrust belt: The effects of sedimentary basin geometry, strain distribution and critical taper, in Sengupta, S., ed., Evo-lution of Geological Structures in Micro- to Macro-scales: London, Chapman and Hall, p. 59–90.
Mitra, S., 2003, A unifi ed kinematic model for the evolu-tion of detachment folds: Journal of Structural Geol-ogy, v. 25, p. 1659–1673, doi: 10 .1016 /S0191 -8141 (02)00198 -0 .
Molinaro, M., Leturmy, P., Guezou, J.C., Frizon de Lamotte, D., and Eshragi, S.A., 2005, The structure and kine-matics of the south-eastern Zagros fold-thrust belt, Iran: From thin-skinned to thick-skinned tectonics: Tectonics, v. 24, TC3007, doi: 10 .1029 /2004TC001633 .
Moores, E.M., Scott, R.B., and Lumsden, W.W., 1968, Ter-tiary tectonics of the White Pine Range–Grant Range region, east-central Nevada, and some regional impli-cations: Geological Society of America Bulletin, v. 79, p. 1703–1726, doi: 10 .1130 /0016 -7606 (1968)79 [1703: TTOTWP]2 .0 .CO;2 .
Nickelsen, R.P., 1963, Fold patterns and continuous defor-mation mechanisms of the central Pennsylvania Appa-lachians, in Cate, A.S., ed., Tectonics and Cambrian–Ordovician stratigraphy in the Central Appalachians of Pennsylvania: Pittsburgh, Pennsylvania, Pittsburgh Geological Society and Appalachian Geological Soci-ety, Guidebook, p. 13–29.
Nolan, T.B., 1962, The Eureka Mining District, Nevada: U.S. Geological Survey Professional Paper 406, 78 p.
Nolan, T.B., Merriam, C.W., and Brew, D.A., 1971, Geo-logic Map of the Eureka Quadrangle, Eureka and White Pine Counties, Nevada: U.S. Geological Survey Miscellaneous Investigations Series Map I-612, scale 1:31,680, 8 p., 2 plates.
Nolan, T.B., Merriam, C.W., and Blake, M.C., Jr., 1974, Geologic Map of the Pinto Summit Quadrangle, Eureka and White Pine Counties, Nevada: U.S. Geo-logical Survey Miscellaneous Investigations Series Map I-793, scale 1:31,680, 14 p., 2 plates.
Nutt, C.J., 2000, Geologic Map of the Alligator Ridge Area, Including the Buck Mountain East and Mooney Basin Summit Quadrangles and Parts of the Sunshine Well NE and Long Valley Slough Quadrangles, White Pine County, Nevada: U.S. Geological Survey Geologic Investigation Series I-2691, scale 1:24,000, 1 plate.
Nutt, C.J., and Hart, K.S., 2004, Geologic Map of the Big Bald Mountain Quadrangle and Part of the Tognini Spring Quadrangle, White Pine County, Nevada: Nevada Bureau of Mines and Geology Map 145, scale 1:24,000, 1 plate.
Oldow, J.S., 1984, Evolution of a late Mesozoic back-arc fold and thrust belt, northwestern Great Basin, U.S.A.: Tectonophysics, v. 102, p. 245–274, doi: 10 .1016 /0040 -1951 (84)90016 -7 .
Otto, B.R., 2008, Geologic Map of the Central Butte Range, White Pine County, Nevada: Nevada Bureau of Mines and Geology Map 160, scale 1:48,000, 1 plate, 8 p.
Overtoom, G.J., 1994, Synvolcanic Oligocene Stress Reori-entation in Eastern Nevada: Evidence from the Golden Gate Range [M.S. thesis]: Salt Lake City, Utah, Uni-versity of Utah, 88 p., 3 plates, scale 1:24,000.
Long
424 Geosphere, April 2015
Perry, W.J., and Dixon, G.L., 1993, Structure and time of deformation in the central Pancake Range, a geologic reconnaissance, in Gillespie, C.W., ed., Structural and Stratigraphic Relationships of Devonian Reservoir Rocks, East-Central Nevada: Reno, Nevada, Nevada Petroleum Society, 1993 Field Conference Guidebook, p. 123–132.
Poole, F.G., 1974, Flysch deposits of Antler foreland basin, western United States, in Dickinson, W.R., ed., Tec-tonics and Sedimentation: Society of Economic Paleon tologists and Mineralogists Special Publication 22, p. 58–82.
Poole, F.G., and Sandberg, C.A., 1977, Mississippian paleogeography and tectonics of the western United States, in Stewart, J.H., Stevens, C.H., and Fritsche, A.E., eds., Paleozoic Paleogeography of the Western United States: Los Angeles, Society of Economic Paleontologists and Mineralogists, Pacific Sec-tion, Pacific Coast Paleogeography Symposium 1, p. 67–85.
Poole, F.G., Stewart, J.H., Palmer, A.R. Sandberg, C.A., Madrid, R.J., Ross, R.J., Jr., Hintze, L.F., Miller, M.M., and Wricke, C.T., 1992, Latest Precambrian to latest Devonian time; development of a continental margin, in Burchfi el, B.C., Lipman, P.W., and Zoback, M.L., eds., The Cordilleran Orogen: Conterminous U.S.: Boulder, Colorado, Geological Society of America, The Geology of North America, v. G-3, p. 9–56.
Quinlivan, W.D., Rogers, C.L., and Dodge, H.W., 1974, Geologic Map of the Portuguese Mountain Quad-rangle, Nye County, Nevada: U.S. Geological Survey Miscellaneous Investigations Series Map I-804, scale 1:48,000, 1 plate.
Ransom, K.L., and Hansen, J.B., 1993, Cretaceous transpressional deformation, Eureka County, Nevada, in Gillespie, C. W., ed., Structural and Stratigraphic Relationships of Devonian Reservoir Rocks, East-Central Nevada: U.S. Geological Survey Nevada Petroleum Society, 1993 Field Conference Guide-book, p. 89–104.
Rich, M., 1977, Pennsylvanian paleogeographic patterns in the western United States, in Stewart, J.H., Stevens, C.H., and Fritsche, A.E., eds., Paleozoic Paleogeogra-phy of the Western United States: Los Angeles, Soci-ety of Economic Paleontologists and Mineralogists, Pacifi c Section, Pacifi c Coast Paleogeography Sympo-sium 1, p. 87–111.
Roberts, R.J., Montgomery, K.M., and Lehner, R.E., 1967, Geology and Mineral Resources of Eureka County, Nevada: Nevada Bureau of Mines and Geology Bul-letin 64, 152 p., 11 plates.
Royse, F., Jr., 1993a, Case of the phantom foredeep: Early Cretaceous in west-central Utah: Geology, v. 21, p. 133–136, doi: 10 .1130 /0091 -7613 (1993)021 <0133: COTPFE>2 .3 .CO;2 .
Royse, F., Jr., 1993b, An overview of the geologic struc-ture of the thrust belt in Wyoming, northern Utah, and eastern Idaho, in Snoke, A.W., Steidtmann, J.R., and Roberts, S.M., eds., Geology of Wyoming: Geological Survey of Wyoming Memoir 5, p. 272–311.
Royse, F., Jr., Warner, M.A., and Reese, D.L., 1975, Thrust belt structural geometry and related stratigraphic problems Wyoming-Idaho–northern Utah, in Bolyard, D.W., ed., Deep Drilling Frontiers of the Central Rocky Mountains: Denver, Rocky Mountain Association of Geologists, p. 41–54.
Schalla, R.A., 1978, Paleozoic Stratigraphy of the Southern Mahogany Hills, Eureka County, Nevada [M.S. thesis]: Corvallis, Oregon, Oregon State University, 118 p., 6 plates.
Simonds, G.G., 1997, Geology and Structural Patterns for the Mountain Boy Range, Eureka County, Nevada [M.S. thesis]: Rapid City, South Dakota, South Dakota School of Mines and Technology, 75 p.
Smith, J., Jr., and Ketner, K.B., 1968, Devonian and Missis-sippian Rocks and the Date of the Roberts Mountains Thrust in the Carlin-Pinon Range Area, Nevada: U.S. Geological Survey Bulletin 1251-I, 18 p.
Snell, K.E., Koch, P.L., Druschke, P., Foreman, B.Z., and Eiler, J.M., 2014, High elevation of the ‘Nevadaplano’ during the Late Cretaceous: Earth and Planetary Sci-ence Letters, v. 386, p. 52–63, doi: 10 .1016 /j .epsl .2013 .10 .046 .
Snyder, R.P., Ekren, E.B., and Dixon, G.L., 1972, Geologic Map of the Lunar Crater Quadrangle, Nye County, Nevada: U.S. Geological survey Miscellaneous Geo-logic Investigations Map I-700, scale 1:48,000, 1 plate.
Speed, R.C., and Sleep, N., 1982, Antler orogeny and fore-land basin: A model: Geological Society of America Bulletin, v. 93, p. 815–828, doi: 10 .1130 /0016 -7606 (1982)93 <815: AOAFBA>2 .0 .CO;2 .
Speed, R.C., Elison, M.W., and Heck, R.R., 1988, Phanero-zoic tectonic evolution of the Great Basin, in Ernst, W.G., ed., Metamorphism and Crustal Evolution of the Western United States, Rubey Volume 7: Englewood Cliffs, New Jersey, Prentice-Hall, p. 572–605.
Stevens, C.H., 1977, Permian depositional provinces and tectonics, western United States, in Stewart, J.H., Stevens , C.H., and Fritsche, A.E., eds., Paleozoic Paleogeography of the western United States: Los Angeles, Society of Economic Paleontologists and Mineralogists, Pacifi c Section, Pacifi c Coast Paleo-geog raphy Symposium 1, p. 113–135.
Stewart, J.H., 1980, Geology of Nevada: A Discussion to Accompany the Geologic Map of Nevada: Nevada Bureau of Mines and Geology Special Publication 4, 136 p.
Stewart, J.H., and Carlson, J.E., 1978, Geologic Map of Nevada: U.S. Geological Survey in collaboration with Nevada Bureau of Mines and Geology, scale 1:500,000, 1 sheet.
Stewart, J.H., and Poole, F.G., 1974, Lower Paleozoic and uppermost Precambrian Cordilleran miogeocline, Great Basin, western United States, in Dickinson, W.R., ed., Tectonics and Sedimentation: Society of Economic Paleontologists and Mineralogists Special Publication 22, p. 28–57.
Stockli, D., Linn, J.K., Walker, J.D., and Dumitru, T.A., 2001, Miocene unroofi ng of the Canyon Range during extension along the Sevier Desert detachment, west central Utah: Tectonics, v. 20, p. 289–307, doi: 10 .1029 /2000TC001237 .
Suppe, J., and Medwedeff, D.A., 1990, Geometry and kine-matics of fault-propagation folding: Eclogae Geologi-cae Helvetiae, v. 83, p. 409–454.
Taylor, W.J., Bartley, J.M., Fryxell, J.E., Schmitt, J., and Vandervoort, D.S., 1993, Mesozoic Central Nevada thrust belt, in Lahren, M.M., Trexler, J.H., and Spinosa, C., eds., Crustal Evolution of the Great Basin and the Sierra Nevada: Boulder, Colorado, Geological Society of America, Cordilleran/Rocky Mountain Sections Field Trip Guidebook, p. 57–96.
Taylor, W.J., Bartley, J.M., Martin, M.W., Geissman, J.W., Walker, J.D., Armstrong, P.A., and Fryxell, J.E., 2000, Relations between hinterland and foreland shortening: Sevier orogeny, central North American Cordillera: Tectonics, v. 19, no. 6, p. 1124–1143, doi: 10 .1029 /1999TC001141 .
Tomastik, T.E., 1981, The Geology of the Southern Part of Buck Mountain, White Pine County, Nevada [M.S. thesis ]: Athens, Ohio, Ohio University, 240 p.
Tracy, W.C., 1969, Structure and Stratigraphy of the Central White Pine Range, East-Central Nevada [M.S. thesis]: Long Beach, California, California State University, 66 p., 8 plates, scale 1:24,000.
Trexler, J.H., Cashman, P.H., Snyder, W.S., and Davydov, V.I., 2004, Late Paleozoic tectonism in Nevada: Tim-ing, kinematics, and tectonic signifi cance: Geological Society of America Bulletin, v. 116, p. 525–538, doi: 10 .1130 /B25295 .1 .
Tschanz, C.M., and Pampeyan, E.H., 1970, Geology and Mineral Deposits of Lincoln County, Nevada: Nevada Bureau of Mines Bulletin 73, 188 p.
Van Buer, N.J., Miller, E.L., and Dumitru, T.A., 2009, Early Tertiary paleogeologic map of the northern Sierra Nevada batholith and the northwestern Basin and Range: Geology, v. 37, p. 371–374, doi: 10 .1130 /G25448A .1 .
Vandervoort, D.S., and Schmitt, J.G., 1990, Cretaceous to Early Tertiary paleogeography in the hinterland of the Sevier thrust belt, east-central Nevada: Geology, v. 18, p. 567–570, doi: 10 .1130 /0091 -7613 (1990)018 <0567: CTETPI>2 .3 .CO;2 .
Villien, A., and Kligfi eld, R.M., 1986, Thrusting and synoro-genic sedimentation in central Utah: in Peterson, J.A., ed., Paleotectonics and Sedimentation in the Rocky Mountain Region, United States: American Associa-tion of Petroleum Geologists Memoir 41, p. 281–308.
Wells, M.L., and Hoisch, T.D., 2008, The role of mantle delamination in widespread Late Cretaceous extension and magmatism in the Cordilleran orogen, western United States: Geological Society of America Bulletin, v. 120, p. 515–530, doi: 10 .1130 /B26006 .1 .
Wiltschko, D.V., and Dorr, J.A., Jr., 1983, Timing of defor-mation in overthrust belt and foreland of Idaho, Wyo-ming, and Utah: American Association of Petroleum Geologists Bulletin, v. 67, p. 1304–1322.
Woodward, L.A., 1962, Structure and Stratigraphy of the Central Egan Range, White Pine County, Nevada [Ph.D. dissertation]: Seattle, Washington, University of Washington, 145 p.
Wyld, S.J., 2002, Structural evolution of a Mesozoic back-arc fold-and-thrust belt in the U.S. Cordillera: New evidence from northern Nevada: Geological Society of America Bulletin, v. 114, p. 1452–1468, doi: 10 .1130 /0016 -7606 (2002)114 <1452: SEOAMB>2 .0 .CO;2 .
Yonkee, W.A., DeCelles, P.G., and Coogan, J.C., 1997, Kinematics and synorogenic sedimentation of the eastern frontal part of the Sevier orogenic wedge, northern Utah, in Link, P.K., and Kowallis, B.J., eds., Proterozoic to Recent Stratigraphy, Tectonics, and Vol-canology, Utah, Nevada, Southern Idaho and Central Mexico: Brigham Young University Geology Studies, v. 42, part 1, p. 355–380.
Young, J.C., 1960, Structure and Stratigraphy in the North-Central Schell Creek Range, Eastern Nevada [Ph.D. dissertation]: Princeton, New Jersey, Princeton Univer-sity, 207 p., 3 plates.