Precambrian Research 236 (2013) 65–84

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Precambrian Research

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Sequence stratigraphy and formalization of the Middle Uinta

Mountain Group (Neoproterozoic), central Uinta Mountains, Utah:

A closer look at the western Laurentian Seaway at ca. 750 Ma

a,∗ a,1 a b

Esther M. Kingsbury-Stewart , Shannon L. Osterhout , Paul K. Link , Carol M. Dehler

a

Department of Geosciences, M.S. 8072, Idaho State University, Pocatello, ID 83209, United States

b

Department of Geology, 4505 Old Main Hill, Utah State University, Logan, UT 83422, United States

a r t a b

i s

c l e i n f o t r a c t

Article history: The mid-Neoproterozoic (ca. 750 Ma) Uinta Mountain Group (UMG), northeast Utah, USA, records trans-

Received 3 November 2012

gressions of an epicontinental sea at least 150 million years before inception of the Laurentian western

Received in revised form 18 June 2013

passive margin. This work refines middle UMG stratigraphy by formalizing three lithostratigraphic

Accepted 20 June 2013

formations and interpreting a sequence stratigraphic framework in the central part of the Uinta Moun-

Available online 19 July 2013

tains. Middle UMG marine and fluvial-deltaic facies associations comprise eight depositional sequences

within a kilometer-thick upward-fining composite sequence. These depositional sequences form one

Keywords:

progradational–aggradational (“lowstand”) sequence set (PASS) and one aggradational–progradational

Neoproterozoic

(“highstand”) sequence set (APSS). Depositional sequences were deposited within a tide- and wave-

Uinta Mountain Group

Rodinia affected epicontinental seaway that received sediment from a south-flowing fluvial system proximally

Laurentia sourced in the Neoarchean southern Wyoming Province to the north and from a separate system of major,

Sequence stratigraphy west-flowing trans-Laurentian rivers distally sourced in the Grenville orogen, the mid-continent granite

Detrital zircon province, and the Yavapai and Mazatzal provinces to the south and east.

Middle UMG fluvial-marine paleogeography strengthens the genetic link with the coeval Big Cotton-

wood and Little Willow formations (Utah), the Chuar Group (Arizona), and upper Pahrump Supergroup

(California), which collectively indicate a ca. 770–740 Ma epicontinental seaway existed across much of

western Laurentia before 700 Ma rifting and 600 Ma formation of the Cordilleran passive margin. Long-

term marine transgression onto continental Laurentia was likely caused by supercontinent breakup,

particularly rifting of the Tarim and South China blocks from the remainder of Rodinia. Poorly con-

strained autocyclic drivers (delta lobe switching, channel avulsion) and allocyclic drivers (climatic

fluctuations, local tectonism) controlled higher frequency depositional cycles superimposed on this long-

term transgression. Western Laurentia thus records prolonged (750–600 Ma) episodic basin formation,

mafic volcanism, and faulting before establishment of a continental terrace after 600 Ma. The Neopro-

terozoic western Laurentian epicontinental seaway can be used as a tie-point with other continents to

help constrain the original continental configuration of Rodinia. Published by Elsevier B.V.

2

1. Introduction Group (UMG), northeast Utah, USA (Fig. 1), making these rocks

among the longest recognized stratigraphic units in North Amer-

The pioneering Powell, King, and Hayden geological surveys of ica (Powell, 1876; Emmons, 1877). Despite its superb exposure,

the mid 1800s first documented the Precambrian Uinta Mountain UMG stratigraphy (and therefore paleogeography) is only grossly

resolved, due to remote location, great thickness, lithologic repe-

tition and related lack of marker units or other regional timelines.

Over 2 km of the middle part of the UMG are exposed in the area of

∗ Kings Peak, Mount Powell, and Red Castle on the crest of the Uinta

Corresponding author at: Wisconsin Geologic and Natural History Survey, Madi-

son, WI, United States. Tel.: +1 608 263 3201; fax: +1 608 262 8086. Mountain anticline (Figs. 1 and 2; Bryant, 1992). Lateral and ver-

E-mail addresses: [email protected] (E.M. Kingsbury-Stewart), tical facies relationships and stratal geometries define a hierarchy

[email protected] (S.L. Osterhout), [email protected] (P.K. Link), [email protected] (C.M. Dehler).

1

Currently with Pioneer Natural Resources, Denver, CO. Research completed

2

while at Idaho State University. Uinta Mountain Group (UMG).

0301-9268/$ – see front matter. Published by Elsevier B.V. http://dx.doi.org/10.1016/j.precamres.2013.06.015

66 E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84

Fig. 1. (A) Regional geologic map of Uinta Mountains, showing Kings Peak and

Mount Powell quadrangles, and localities mentioned in the text. Modified after

Haddox et al. (2005). (B) Simplified geologic map of north-central Uinta Mountains in

the area of the Kings Peak and Mount Powell quadrangles. Boxes locate stratigraphic

sections shown in Fig. 5. Triangles locate major mountain peaks. Zuc = Red Castle For- Fig. 2. Photopanel of the east wall of the Henry’s Fork drainage above Dollar Lake

mation; Zuda = Dead Horse Pass and Mount Agassiz formations; Zuh = formation of showing stratal geometry and stratigraphic units. The box shows the zoomed-in

Hades Pass. Base from D. Sprinkel, Utah Geological Survey, unpublished, with Kings area. The arrow points towards south. DS = Depositional sequence. Zuc: Red Castle

Peak and Mount Powell quadrangles simplified from our mapping (Kingsbury, 2008; Formation; Zud: Dead Horse Pass Fm.; Zuma: Mount Agassiz Fm.

Osterhout, 2011).

Farmer, 1998; Condie et al., 2001; Dehler et al., 2010). The active

of marine and marine through fluvial-deltaic successions that are

northern margin of the half-graben was bounded by reactivated

exposed, often in three dimensions, above tree line along later-

structures along or south of the southern edge of the Archean

ally continuous (km-scale) cirque walls along the crest of the Uinta

Wyoming Province (Sears et al., 1982; Bryant and Nichols, 1988;

Mountains (Figs. 1 and 2). These exposures are only found in the

Stone, 1993; Nelson et al., 2002, 2011). Neoproterozoic normal

remote parts of the range and offer insight into the more detailed

faulting accompanied UMG deposition (Brehm, 2008; Kingsbury,

nature of the UMG strata, therefore enhancing paleoenvironmental

2008; Rybczynski, 2009). Paleomagnetic studies suggest a near-

and paleogeographic understanding of the UMG.

equatorial paleolatitude (Weil et al., 2004, 2006).

Our goal is to integrate several independent observations from

Latest Neoproterozoic to early Cambrian normal faulting tilted

the middle UMG in the middle part of the Uinta Mountain range

and uplifted the UMG prior to deposition of Paleozoic strata (Stone,

including detrital zircon age spectra, lithofacies and facies associ-

1993; Bryant, 1992). Extensional structures within the UMG basin

ations, vertical stacking patterns, and stratal architecture exposed

were inverted during Paleozoic contractional events, for example

in outcrop to resolve the lithostratigraphy and sequence stratig-

the late Pennsylvanian – early Permian Ancestral Rocky Moun-

raphy of the middle UMG. Specifically, we (1) formalize three

tains orogeny (Stone, 1993). Structural inversion and growth of

geologic units (the Red Castle, Dead Horse Pass and Mount Agassiz

the modern Uinta Mountains culminated in the Late Cretaceous to

formations) to facilitate stratigraphic understanding of the Neo-

mid-Cenozoic Laramide orogeny (Bradley, 1995; DeCelles, 2004).

proterozoic section in the Uinta Mountains; (2) characterize UMG

The UMG unconformably overlies Paleoproterozoic metamor-

stratigraphy in terms of a hierarchy of accommodation-succession

phic rocks along the northeastern edge of the Uinta Mountains

(sensu Neal and Abreu, 2009); and (3) integrate these new data into

(Hansen, 1965; Sears et al., 1982), but the base is not exposed in

the regional understanding of the Neoproterozoic paleogeography

the west (e.g., Wallace, 1972). Cambrian or Mississippian strata

of western Laurentia.

unconformably overlie the UMG (Hansen, 1965).

The quartzose and arkosic UMG has been interpreted as a

2. Geologic setting sand-dominated, fluvial (Sanderson, 1978, 1984; Condie et al.,

2001); fluvial-marine (Wallace and Crittenden, 1969; Wallace,

The upper Precambrian (Neoproterozoic, Cryogenian) Uinta 1972; Dehler et al., 2010), or fluvial-lacustrine (Link, 1993; Winston

Mountain Group contains up to 7 km of mainly red-colored and Link, 1993) system within an elongate basin that opened to the

sandstone and mudrock, and is only exposed in the Uinta Moun- west and south (e.g. Hansen, 1965; Wallace and Crittenden, 1969;

tains of northern Utah (Hansen, 1965;Fig. 1). Previous workers Dehler et al., 2010). The UMG contains three, km-thick, upward-

have suggested deposition in an intracratonic half-graben with fining composite sequences (depositional sequences of Dehler et al.,

an east-west-trending northern margin (Hansen, 1965; Ball and 2010; Fig. 3). The lower composite sequence is only exposed in the

E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84 67

Fig. 3. Generalized stratigraphic columns from the eastern and western Uinta

Mountains. Composite sequence boundaries divide the Uinta Mountain Group

into three major composite sequences. Abbreviations: CS, composite sequence;

CSB, composite sequence boundary; CTS, composite transgressive surface; Deadhs.,

Deadhorse Pass Formation; lower RC, lower member of the Red Castle Formation;

Fig. 4. Simplified stratigraphic columns of Kings Peak and Mount Powell quad-

middle RC, middle member of the Red Castle Formation; Moosehorn, formation of

rangles showing formally defined Red Castle, Dead Horse Pass, and Mount Agassiz

Moosehorn Lake; Mt. Ag., Mount Agassiz Formation; Mt. W., Mount Watson Forma-

formations and sequence stratigraphic terminology used in this paper.

tion; upper RC, upper member of the Red Castle Formation. Figure modified from

Dehler et al. (2010).

et al., 2000) provides a young age-bound for the upper composite

sequence (Dehler et al., 2001a).

eastern part of the range, some 100–160 km southeast of the study

The UMG has long been thought to be correlative with the partly

area, and includes the conglomeratic Jesse Ewing Canyon Forma-

tidal Big Cottonwood Formation (Wallace and Crittenden, 1969;

tion and the informal formations of Diamond Breaks and Outlaw

Crittenden and Wallace, 1973; Link, 1993; Chan et al., 1994; Ehlers

Trail (De Grey, 2005; De Grey and Dehler, 2005). One detrital-

et al., 1997; Ehlers and Chan, 1999; Dehler et al., 2001b, 2010;

zircon sample from the Outlaw Trail unit contains four zircons (out

Link and Christie-Blick, 2011) and has recently been shown to also

of ∼128 total grains) with ages of 726 ± 56; 721 ± 54; 804 ± 46;

be correlative with the metamorphosed Little Willow Formation

and 801 ± 52 Ma (see data repository of Dehler et al., 2010). Dehler

(Spencer et al., 2012) in the Wasatch Range of northern UT. Neo-

et al. (2010) report these grains to be within analytic uncertainty

proterozoic ages (750–850 Ma) from detrital zircons in the Little

of each other with a concordia age of 766 ± 4.8 Ma (mean square of

Willow Formation and similar detrital zircon age populations from

weighted deviates is 0.66), which is the best (and only) constraint

the Little Willow and Big Cottonwood formations of the Wasatch

on the maximum age of the entire Group (Fig. 3; Dehler et al., 2007,

Range support this correlation (Spencer et al., 2012).

2010). Other ca. 800 Ma detrital zircons have been found in small

numbers in the Jesse Ewing Canyon Formation and the formation of

Moosehorn Lake (Dehler et al., 2010; Fig. 3). Composite sequence 3. Formalization of units

two, the focus of this paper, includes the Red Castle, Dead Horse

Pass, and Mount Agassiz formations, which make up the high spine Previous work in the UMG (Wallace and Crittenden, 1969;

of central part of the range (Figs. 3 and 4), the informal formation Wallace, 1972; Sanderson, 1978) established informal stratigraphic

of Moosehorn Lake (not exposed in the study area), and the infor- units (i.e. “formation of Red Castle”) that were not formally

mal formation of Crouse Canyon in the east. Composite sequence defined to the specifications of the North American Stratigraphic

three includes the informal formation of Hades Pass and the overly- Code (North American Commission on Stratigraphic Nomenclature,

ing Red Pine Shale, which contains microfossil assemblages similar 2005). We here adopt and formalize the Red Castle, Dead Horse

to those found in the Chuar Group in the Grand Canyon (Fig. 3; Pass, and Mount Agassiz formations (Tables 1 and 2, Data Reposi-

Dehler et al., 2007). Correlation of the UMG with the Chuar Group, tory Appendices 1 and 2). These formal units are used in geologic

◦ ◦

which contains an ash bed with an age of 742 ± 6 Ma (Karlstrom maps of the western UMG, including the Salt Lake 1 by 2 ,

68 E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84

Table 1

Table showing the development of the stratigraphic nomenclature for the western Uinta Mountain Group. Each column represents a publication (bold text) that first informally

named or formalized a lithostratigraphic unit in the western UMG. The units that each publication discusses, whether first informally or formally defined or simply adopted

from previous studies, are listed in the column under the publication. Formalization of an informal unit by a subsequent study is indicated by the name change from ‘formation

of. . .’ to ‘. . . Formation’. For example, Sanderson (1978) formalized the Mount Watson Formation, which was first informally defined by Wallace (1972) and Crittenden and

Wallace (1973). The relationship between lithostratigraphic and sequence stratigraphic units is also shown.

Williams (1953) Wallace (1972), and Sanderson (1978) This study Sequence stratigraphic

*,+

Crittenden and Wallace hierarchy see Figs. 3–5

(1973)

Red Pine Shale Red Pine Shale Red Pine Shale Red Pine Shale Composite sequence 3

formation of Hades Pass formation of Hades Pass formation of Hades Pass formation of Hades Pass Composite sequence 3

formation of Mount Mount Watson Formation Mount Watson Formation Composite sequence 2

Watson

formation of Mount Mount Watson Formation Mount Agassiz Formation Composite sequence 2

Agassiz

Depositional sequences 6-8

formation of Dead Horse Mount Watson Formation Dead Horse Pass Formation Composite sequence 2

Pass

Depositional sequences 4–5

formation of Moosehorn formation of Moosehorn formation of Moosehorn Composite sequence 2

Lake Lake Lake

Uinta Mountain Group formation of Moosehorn Composite sequence 2

undivided Lake

formation of Red Castle formation of Red Castle Red Castle Formation Composite sequence 2

(upper member)

Depositional sequences 3–6

Red Castle Formation Composite sequence 2

(middle member)

Depositional sequence 3

Red Castle Formation Composite sequence 2

(lower member)

includes Island Lake Depositional sequences 1–2

quartzite tongues

*

sensu Neal and Abreu (2009).

+

Composite sequences revised from Depositional sequences of Dehler et al. (2010).

 

Kings Peak 7.5 , and Mount Powell 7.5 quadrangles (Bryant, 1992; arenite. The basal contact of the Dead Horse Pass Formation and

Kingsbury, 2008; Osterhout, 2011, respectively). Reference sections the equivalent upper member, Red Castle Formation is a map-

are shown in Fig. 5 and described in Appendices 1 and 2 in the pable stratigraphic discontinuity (composite transgressive surface

Data Repository. We did not formalize the formation of Hades Pass 1, see Section 5, Fig. 5) that separates fine-grained strata above,

because it is not fully exposed within the study area. Sequence from coarse-grained, angular, poorly sorted arkosic sandstone,

stratigraphic surfaces and geometries referenced in this section are below.

formally presented under section 5.

3.3. Mount Agassiz Formation

3.1. Red Castle Formation

The Mount Agassiz Formation (159 m) overlies the Dead Horse

The Red Castle Formation is subdivided into three informal Pass Formation, contains upward-coarsening mudstone through

members and contains at least 735 m of reddish, conglomeratic, tabular quartz arenite, and is generally finer-grained than the

feldspathic arenite and subordinate siltstone. The lower member underlying Dead Horse Pass Formation. The basal contact is a stratal

contains at least 150 m of arkosic sandstone (up to 50% k-feldspar) discontinuity (SBe; Fig. 5, see Section 5, Sequence Stratigraphy)

and several meters-thick, tabular quartz arenite interbeds that we overlain by a distinctive, red- weathering siltstone at its type local-

informally name the Island Lake quartzite tongues (Figs. 4 and 5). ity (Table 2). The Mount Agassiz Formation undergoes a facies

The base is not exposed. The middle member contains at least change, grading westward into red, coarser- grained, feldspathic

275 m of tabular-bedded arkosic sandstone and sparse quartz sandstone and siltstone of the upper part of the upper member,

arenite interbeds. The upper member contains at least 350 m of Red Castle Formation. The top of the Mount Agassiz Formation and

upward-coarsening mudstone through lenticular-bedded arkosic the upper member, Red Castle Formation is a regionally mappable,

sandstone. The upper member of the Red Castle Formation under- stratal discontinuity (composite sequence boundary 3, Fig. 5, see

goes a facies change to the east, grading into finer-grained Section 5) that incises underling strata and is overlain by coarse-

sediments of the Dead Horse Pass and Mount Agassiz formations grained, pebbly, lenticular-bedded quartzose sandstone of the base

(Fig. 5). In the west an erosive contact separates tabular-bedded, of the formation of Hades Pass.

arkosic arenite (tabular arkose lithofacies, see Section 5.1, Table 3,

Fig. 5) of the upper member from lenticular-bedded sub-arkosic

4. Detrital zircons

to quartz arenite (lenticular quartzose lithofacies, see Section 5.1,

Table 3, Fig. 5) of the overlying formation of Hades Pass.

To determine the provenance of the middle UMG, we obtained

Laser Ablation Inductively Coupled Plasma Mass Spectrometer (LA-

3.2. Dead Horse Pass Formation ICP MS) detrital zircon data from five new samples from diverse

lithofacies (described in detail below under Section 5) in the central

The Dead Horse Pass Formation contains at least 150 m of Uinta Mountains (Supplementary Table S1). New samples include

upward-coarsening mudstone, through tabular-bedded quartz two from the Island Lake quartzite tongue of the lower member,

E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84 69

Table 2

Formalization of units.

Name Red Castle Formation

Name derivation Type area located near the Red Castle; Smiths Fork basin; Mount Powell quadrangle

Category & rank lithostratigraphic Formation

Type area Head of Smiths Fork basin, near the Red Castle (Wallace, 1972). The type location for the Island Lake quartzite tongue is Island

Lake in the Mount Powell quadrangle (12T0550780 4518713 elev. 10854).

Unit & boundary reference section - W. and NW of the Red Castle

- UTM 12 T 0544630 4516405; 12 T 0543704 4516517; 12 T 0542704 4519264

- Lower boundary: unexposed

- Upper boundary: erosive surface (CSB 3) separating the Red Castle Formation (below) and formation of Hades Pass (above).

- W. boundary: gradational into the Mount Watson Formation

- E. boundary: gradational contact with the Dead Horse Pass and Mount Agassiz formations

Lower boundary reference location Unexposed lower boundary

Unit description Divided into 3 informal members: (1) lower member: meters-thick interbeds of arkose and quartz arenite. Arkose is red to

purple, texturally and compositionally immature and organized in decimeter-thick, lenticular beds with erosive, concave

bases that pinch into sharp, planar top surfaces rarely capped by cm-thick, planar laminated, sandy siltstone. Quartz arenite is

either (a) purple to tan, well to subrounded, well sorted, medium- to coarse-grained, quartz to subarkosic with lesser silty

sandstone and sandy siltstone and organized in tabular to broadly lenticular or sigmoidal beds; or (b) purple to tan

fine-grained sandstone that fines upward into siltstone and occasionally is capped by cm-thick shale. The base of the lower

member is not exposed. The top of the member is sharp (erosive) to gradational into the middle member. The contact is

placed (when not eroded away) at the first laterally continuous red, silty shale between lenticular arkosic and tabular arkosic

arenite; (2) middle member: arkose and rare fine-grained interbeds. Arkose is laterally continuous (100s of meters), tabular,

upward-fining, texturally and compositionally immature, 10 to 50cm-thick, red to purple arkose/gray silt couplets with sharp

upper and basal contacts. Mud rip-up clasts and occasional 0.5 to 1 cm scale euhedral feldspar clasts are common, especially

at the base of couplets. Fine-grained interbeds are laterally continuous (10s to 100s of meters), decimeter- to meters-thick,

black to green, laminated clay-shale to siltstone and lesser fine-grained, wavy-laminated sandstone and a low diversity fossil

assemblage of acritarchs Leiosphaeridia sp. and organic filaments or black to tan, fine-grained, parallel and wavy laminated or

hummocky cross stratified sandstone and siltstone with lesser clay-shale.The upper contact of the middle member is sharp to

erosional with the upper member. The contact is placed between tabular arkoisc arenite beds and the first purple mature

quartz arenite or dark green interbedded fine-grained sandstone and sandy siltstone; (3) upper member: similar to middle

member except fine-grained interbeds are thicker and more common.

Dimensions Greater than 720 m (Wallace, 1972), greater than 735 m at reference section

Geologic age Neoproterozoic (∼740–770 Ma, Dehler et al., 2010)

Correlations The Red Castle Formation may pass into the Mount Watson Formation (W. Uinta Mountain Group)

Name Dead Horse Pass Formation Mount Agassiz Formation

Name derivation Dead Horse Pass, between the Blacks Fork and Rock Creek Mount Agassiz, a prominent peak at the head of the east fork of

basin, W. Uinta Mountains, Explorer Peak quadrangle the Duchesne River, W. Uinta Mountains, Hayden Peak

quadrangle

Category/rank Lithostratigraphic Formation Lithostratigraphic Formation

Type area 1.5 km south of Dead Horse Pass, head of Rock Creek Range crest between the Duchesne and Uinta Rivers (Wallace,

(Wallace, 1972) 1972)

Unit & boundary reference section - S. flank, Gilbert Peak (UTM 12 T 0554681/4519960 NAD - S. flank, Gilbert Peak (UTM: 12 T 0554681/4519960 NAD 27)

27)

- Lower boundary: erosive surface (CTS1, see Fig. 5) - Lower boundary: sharp/erosive surface (SB e)

- Upper boundary: sharp/erosive surface (SB e, see Fig. 5) - Upper boundary: sharp/erosive surface (CSB 3, see Fig. 5)

below fm. Hades Pass

- W. boundary: gradational into upper member, Red Castle - W. boundary: gradational into upper mbr., Red Castle Fm.

Fm.

- E. boundary: faulted contact with overlying fm. of Hades - E. boundary: faulted contact with overlying fm. of Hades Pass

Pass (?) (?)

Lower boundary reference location - Erosive/sharp surface (CTS1) between Red Castle Fm. - Erosive surface (SB e) between Dead Horse Pass Fm. (below)

(below) and Dead Horse Pass Fm. (above). and distinctive red, subfeldspathic fine-grained sandy siltstone

(above).

- E. wall, Henry’s Fork drainage above Dollar Lake (UTM: - E. wall, Henry’s Fork basin at Dollar Lake (UTM: 12 T

12 T 0553278/4520439 (NAD 27) 0553278/4520439 NAD 27)

- E. wall, Kings Peak (UTM: 12 T 0553635/4513968 NAD 27)

Unit description Decameter-thick upward-coarsening fine-grained to Decameter-thick upward-coarsening couplets similar to the

sandstone couplets. Fine-grained rocks are laterally Dead Horse Pass Fm. The Mount Agassiz Fm. is distinguished

continuous (10s to 100s of meters), meters- to rarely from the Dead Horse Pass Fm. by the thicker and more

decameters-thick, black to green, laminated clay-shale to common presence of interbedded, decimeter-thick gray

siltstone and lesser fine-grained, wavy-laminated laminated shale and black, pink, or tan fine-grained sandstone

sandstone and a low diversity fossil assemblage of that fines upward into siltstone and rarely is capped by

acritarchs Leiosphaeridia sp. and organic filaments; or red cm-thick shale. The Mount Agassiz is also typically lighter

to black to tan, fine-grained, parallel and wavy laminated beige to white in color.

or hummocky cross stratified sandstone and siltstone with

lesser clay-shale. Sandstone is either (a) purple to tan, well

to subrounded, well sorted, medium- to coarse-grained,

quartz to subarkosic with lesser silty sandstone and sandy

siltstone and organized in tabular to broadly lenticular or

sigmoidal beds; or (b) interbedded, decimeter-thick gray

laminated shale and black, pink, or tan fine-grained

sandstone that fines upward into siltstone and rarely is

capped by cm-thick shale. Refer to Appendix A for a

complete stratigraphic column of the Dead Horse Pass Fm.

at the reference section (S. flank, Gilbert Peak).

70 E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84

Table 2 (Continued )

Name Dead Horse Pass Formation Mount Agassiz Formation

Refer to Appendix A for a complete stratigraphic column of the

Mt. Agassiz Fm. at the reference section (s. flank, Gilbert Peak).

Dimensions 340 m to 490 m thick at type area (Wallace, 1972) 310 m to 460 m thick in the type area (Wallace, 1972)

153 m thick at unit reference section (Kingsbury, 2008; 165 m thick at unit reference section (Kingsbury, 2008; refer to

refer to Appendix A for a complete stratigraphic column at Appendix A for a complete stratigraphic column at the

the reference section, s. flank, Gilbert Peak) reference section, s. flank, Gilbert Peak)

Geologic age Neoproterozoic (∼740 - 770 Ma, Dehler et al., 2010) Neoproterozoic (∼740 - 770 Ma, Dehler et al., 2010)

Correlations - Red Castle Fm. (W. Uinta Mountain Group) - Red Castle Fm. (W. Uinta Mountain Group)

- The Dead Horse Pass Fm grades into the Red Castle Fm. at - The Mount Agassiz Fm. grades into the Red Castle Fm. at the

the head of the Henrys Fork basin, near the boundary head of the Henrys Fork basin, near the boundary between the

between the Kings Peak and Mount Powell quadrangles. Kings Peak and Mount Powell quadrangles.

Red Castle Formation (tabular quartzose lithofacies, Figs. 5 and 6e the probability-density curve, and ages of populations were gener-

and g); one from the lower member, Red Castle Formation (lentic- alized visually. The number of zircons analyzed is shown on each

ular arkose lithofacies, Fig. 6f); one from the middle member, plot. Most (over 97%) grains are less than 10% discordant.

Red Castle Formation (tabular arkose lithofacies, Fig. 6d); and one

from the upper member, Red Castle Formation (siltstone lithofa-

cies, Fig. 6b). The five new samples are displayed together in Fig. 6 4.2. Observations and interpretations

with two previously reported Sensitive High Resolution Ion Micro-

probe (SHRIMP) data sets from the lowermost Dead Horse Pass We recognize two provenance signatures in the detrital zircon

Formation (siltstone lithofacies, Fig. 6c) and the formation of Hades age spectra. One provenance signature is characterized by mixed

Pass (lenticular quartzose lithofacies, Fig. 6a) (data in Dehler et al., Proterozoic and Archean age components. The other provenance

2010). signature is characterized by a dominant Neoarchean peak. These

patterns are consistent with previous UMG provenance studies

(Mueller et al., 2007; Dehler et al., 2010).

4.1. Methods Four of the new detrital zircon samples and both of the pre-

viously reported samples (Dehler et al., 2010) have the mixed

The detrital zircon mineral separates were produced from sev- provenance signature. The lowest exposed quartz sandstone of the

eral kg of fine- and medium-grained sandstone. A heavy mineral Island Lake tongue (2SL10, Fig. 6g) has large zircon age peaks at

concentrate was prepared from the total rock using standard crus- 1035 and 1070 Ma, within a broad distribution from 950 to 1170

hing, washing, heavy liquid (Sp. Gr. 2.96 and 3.3), and paramagnetic Ma that makes up 75% of the sample. There is a small peak (10%)

procedures (Williams, 1998). at 1620 Ma and scattered older Paleoproterozoic and Neoarchean

U-Pb geochronology was conducted in 2010 and 2011 by laser grains. The overlying arkosic sandstone (3SL10, Fig. 6f) also has

ablation multicollector inductively coupled plasma mass spectrom- mixed detrital zircon ages, with peaks at 1075 and 1190 Ma. Grains

etry (LA-MC-ICPMS) (Gehrels et al., 2006, 2008, 2011). One hundred 1025–1200 Ma make up 42% of the sample. Grains between 1400

random zircon grains from each sample were ablated with a New and 1900 Ma make a scattered distribution. The only older peak is

Wave UP193HE Excimer laser using a spot diameter of 30 m. All at 2630 Ma. The overlying quartzose Island Lake tongue (27PL08,

measurements were made in static mode, using Faraday detectors. Fig. 6e) has age-peaks at 1090 and 1200 Ma, with 58% of the grains

Each analysis consisted of one 15-second integration on peaks with between 1000 and 1200 Ma. There is a prominent grouping (23% of

the laser off (for backgrounds), 15 one-second integrations with the the grains) at 1360–1400 Ma and scattered Paleoproterozoic and

laser firing, and a 30 second delay to purge the previous sample Archean grains. Sandy siltstone of the upper member, Red Cas-

and prepare for the next analysis. The ablation pit was ∼15 m in tle Formation (5SL10, Fig. 8b) has a wide grain-age distribution,

depth. with peaks at 1090 and 1190 Ma, within a grouping from 1000 to

206 238

For each analysis, the errors in determining Pb/ U and 1200 Ma that includes 47% of the grains. There are also age-peaks

206 204

Pb/ Pb result in a measurement error of ∼1–2% (at 2- at 1255 and 1890 Ma, within a distributed set of grains as old at

206 238

sigma level) in the Pb/ U age. The errors in measurement of 2700 Ma. The stratigraphically highest sample is shown in Fig. 6a

206 207 206 204

Pb/ Pb and Pb/ Pb also result in ∼1–2% (at 2-sigma level) and is from the formation of Hades Pass (31PL06, SHRIMP data).

uncertainty in age for grains that are > 1.0 Ga, but are substantially This sample has distributed Proterozoic grain ages with 30% of the

207

larger for younger grains due to low intensity of the Pb signal. grains from 1000 to 1200 Ma and small Archean peaks at 2560 and

206 238

The Pb/ Pb age is used for grains (sparse in the present study) 2625 Ma.

less than 1000 Ma. Common Pb correction was accomplished by Two of the detrital zircon samples have mainly Archean pro-

using Hg-corrected Pb and assuming an initial Pb composition from venance signatures. A fine-grained arkosic sandstone in the middle

Stacey and Kramers (1975). member of the Red Castle Formation (22SL10; Fig. 6d) has a uni-

Inter-element fractionation of Pb/U is generally ∼5%, whereas modal Archean age peak at 2630 Ma, with 100% of the grains

apparent fractionation of Pb isotopes is generally < 0.2%. In-run between 2560 and 2720 Ma. The fine-grained, feldspathic arenite of

analysis of fragments of a large zircon crystal (every fifth mea- the Deadhorse Pass Formation (36PL06, SHRIMP, Fig. 6c) is compa-

surement) with known age of 563.5 ± 3.2 Ma (2-sigma error) was rable, with scattered Proterozoic grains and a strong Archean peak

used to correct for this fractionation. The uncertainty resulting at 2620 Ma. Archean grains make up 66% of the non-discordant

from the calibration correction is generally 1–2% (2-sigma) for both grains.

206 207 206 238

Pb/ Pb and Pb/ U ages. In general, the provenance of the observed Proterozoic age-

The data were reduced using the Isoplot Excel Macro of Ludwig peaks are interpreted as follows: 1000–1200 Ma populations are

(2003). The number of grains shown on the plots of Fig. 6 rep- Grenvillean, e.g. Mueller et al. (2007); 1340–1430 Ma grains were

resents only analyses less than 10% discordant and 5% reverse derived from A-type mid-continent granites (Anderson, 1989);

discordant. The detrital zircon age peaks were picked directly from 1650–1890 Ma Paleoproterozoic grains were derived from the

E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84 71

Table 3

Summary of formations, lithofacies, and facies associations.

Formation Lithofacies Lithology/grain size Bedding and structures Interpretation Association

Lithofacies

Upper mbr., Red Offshore to lower shoreface marine

Castle Fm.; Dead

Horse Pass Fm.;

Mount Agassiz

Fm.

Mudstone Black to green, fissile, Laterally continuous (10s–100s m); parallel laminated shale; offshore, below

clay-shale to siltstone; rare wavy laminated sandstone and near storm

fine-grained sandstone; wave base.

low diversity fossil

assemblage of acritarchs

Leiosphaeridia sp. and

organic filaments

Siltstone Black to tan fine-grained Laterally continuous (>100s m); parallel and wavy laminations Lower shoreface

sandstone and interbedded (Fig. 7D), hummocky cross stratification (Fig. 7A) near storm wave

siltstone, lesser clay-shale base; offshore-transition

zone

Island Lake tongues Upper shoreface and nearshore marine

of lower mbr.,

Red Castle Fm.;

Dead Horse Pass

Fm.; Mount

Agassiz Fm.

Tabular quartzose Well to sub-rounded, well Laterally continuous (>100’s m); tabular to broadly lenticular Upper shoreface

sorted, medium to beds; occasional decameter-scale foresets (Fig. 7C); current marine/nearshore

coarse-grained, quartz to and wave ripples; mudcracks; planar-tabular and trough and possibly

sub-arkosic arenite; lesser cross-beds; soft sediment deformation associated with estuarine

fine-grained sandstone and lenticular beds; occasionally massive. Gross upward-fining

siltstone; occasional shale trend (>100 m) from Dead Horse Pass to Mt. Agassiz Fms.:

caps Fine-grained interbeds increase upsection; decimeter-thick

fine-grained sandstone with mud-chips, current ripples, and

lesser flaser bedding (Fig. 7E) and shale interbeds fine upward

into siltstone with occasional shale caps. West-directed

(Mount Agassiz Fm.) and southeast directed (Island Lake

tongue) paleocurrents (Fig. 5).

Lower (excluding Deltaic

the Island Lake quartzite

tongues), middle

and upper mbrs.,

Red Castle Fm.

Tabular Arkose Red, angular to subangular, Laterally continuous (>100s m), tabular, upward-fining braid bars on a

poorly sorted, coarse- sand/siltstone couplets (10-50cm-thick scale), with sharp broad, flat,

grained feldspathic arenite upper and basal contacts; current ripples truncated at regular well-developed

to feldspar-rich pebble intervals by reactivation surfaces and often overlain by mud tidally-influenced

conglomerate with drapes; whole preservation of cm-scale dunes; climbing braid-delta

interbedded siltstone and ripples; mud rip-up clasts; soft sediment deformation;

silty sandstone. occasional 0.5 to 1cm-scale, euhedral feldspar clasts

concentrated along bed bases; bidirectional

north/south-directed paleoflow (Fig. 5); interbedded with the

siltstone lithofacies; decrease in siltstone lithofacies interbeds

from east to west of study area (fig. 5)

Lenticular arkose similar to tabular arkose Amalgamated, sub-meter to meter-thick lenticular beds with braid bars of a

with lesser textural and erosive, concave bases that pinch into sharp, planar upper tidally influenced

compositional maturity; surfaces (channel forms) and are rarely capped by cm-thick, braid-delta

reworked quartz arenite planar laminated, sandy siltstone (Fig. 7J). Lenticular beds fine

clasts upward from granual-bearing very coarse-grained sandstone

to medium-grained, cross-bedded sandstone and contain mud

rip-up clasts and 0.5 to 1 cm, euhedral feldspar clasts. The

lenticular arkose lithofacies repeatedly overlies the tabular

quartzose lithofacies across an erosive lower contact (Fig. 7F).

Siltstone clasts from the tabular quartzose lithofacies are

reworked into the bases of lenticular arkose beds.

Lowermost fm. of Fluvial

Hades Pass

Lenticular Red, sub-angular to well Amalgamated, decimeter-thick lenticular beds with erosive, Braided fluvial

quartzose rounded, poorly to well concave bases that pinch into sharp, planar top surfaces

sorted, medium- to (channel forms) often capped by cm-thick, planar-laminated

coarse-grained quartz to sandy siltstone (Fig. 7L); internally massive beds or trough

◦ ◦

feldspathic arenite and crossbeded,; abundant cm-scale steeply inclined (∼30 - 40 ),

lesser siltstone wedge-shaped accretion surfaces; current ripples; soft

sediment deformation; slump folds; abundant secondary

alteration; southeast-directed paleoflow (Fig. 5). Transitions

into the lenticular arkose lithofacies to the west.

72 E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84

Fig. 5. Measured stratigraphic sections including paleocurrents and sequence stratigraphic interpretation for the Red Castle, Dead Horse Pass and Mount Agassiz formations.

Measured sections are reference sections for the newly formalized Dead Horse Pass and Mount Agassiz formations. Sequence stratigraphic terminology used in the text is

shown on measured sections. A transgressive surface and sequence boundaries, traceable on cliff walls over several kilometers, serve as lines of correlation between the two

quadrangles. Descriptions of measured sections can be found in Data Repository Appendices 1 & 2.

Yavapai-Mazatzal Provinces (Karlstrom and Bowring, 1993. Con- fluvial system draining the Neoarchean southern Wyoming

sistent with Dehler et al. (2010) and Spencer et al. (2012), Province (Wallace, 1972; Mueller et al., 2007). The southern

we interpret that these Proterozoic components were deliv- Wyoming Province is characterized by detrital zircon age spectra

ered by transcontinental rivers from southern and/or eastern (age peaks at 2627, 2681, and 2727 Ma, see Fig. 2 of Shufeldt et al.,

Laurentia. 2010) that very closely match the Neoarchean ages we report (age

In contrast, we interpret the two mainly Archean age distribu- peaks at 2560, 2625, 2620, 2630, and a cluster around 2700 Ma).

tions (Fig. 6c and d) to have been derived from a south-flowing Furthermore, these two samples with the highest percentage of

E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84 73

Fig. 6. Probability-frequency plots for seven detrital zircon samples representing the exposed stratigraphic section in the Uinta Mountain Group from the north-central

Uinta Mountains. Plots are arranged stratigraphically with the oldest (letter g) at the bottom of the diagram. Selected age-peaks are shown and generalized from the

probability-density curve. Plots a and c are from Dehler et al. (2010). Plots b and d through g contain new data presented in this paper (Supplementary data Table S1).

Neoarchean grains are also the most arkosic, as would be expected young as 2.2 Ga), and do not form the clean 2.6 and 2.7 Ga peaks

from north-derived fluvial systems draining the proximal south- present in the arkosic Uinta Mountain Group.

ern Wyoming craton, where Neoarchean granites are extensive

(Mueller and Frost, 2006). Although Neoarchean detrital grains in

5. Sequence stratigraphy

the Paleoproterozoic Vishnu Schist of the Grand Canyon are thought

to be sourced from the Mojave Province (Shufeldt et al., 2010), We use 1:24,000 field mapping of the Mount Powell and

the ages from the Vishnu span Neoarchean to Paleoproterozoic (as Kings Peak 7.5 min quadrangles, lithofacies and facies associations,

74 E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84

vertical stacking patterns, stratal geometries, and stratal termi- without any implied relationship between systems tracts and

nations (onlap, downlap, and truncation) to identify a sequence the shelf edge or sea level. The terms ‘highstand’ and ‘low-

stratigraphic hierarchy comprising eight depositional sequences stand’ imply a relationship between systems tracts and the sea

that stack to form one nearly complete composite sequence (sensu level curve, which is unresolved for the Neoproterozoic, while

Neal and Abreu, 2009). Lithofacies, vertical stacking patterns, and the terms ‘APD’ (aggradation–progradation–degradation) and ‘PA’

stratal geometries are displayed in spectacular, panoramic cirque (progradation–aggradation) objectively describe the surfaces and

wall exposures and documented in Figs. 2, 7–10. Vertical forestep- stratal geometries that make up the physical rock record. Further-

ping and backstepping facies relationships observed in measured more, use of accommodation-succession terminology allows us to

section are exhibited in Fig. 5. describe a hierarchy of higher-frequency depositional sequences

We interpret a sequence stratigraphic framework in terms nested within a lower-frequency sequence while avoiding defin-

of a hierarchy of accommodation-succession following Neal ing stratigraphic cycle order in the absence of high-frequency age

and Abreu (2009). We interpret lithofacies and facies asso- control. The hierarchical framework of Neal and Abreu (2009)

ciations, vertical staking patterns, and stratal geometries and is, from small-scale to large-scale: parasequence, systems tracts,

terminations using the accommodation succession terminology depositional sequence, sequence set, composite sequence, com-

of Neal and Abreu (2009) because this terminology describes posite sequence set, and megasequence. We document a sequence

the hierarchy of sedimentary units based entirely on geometry stratigraphic hierarchy for the middle UMG consisting of system

Fig. 7. Photographs of facies associations (2 pages). (A–F) offshore to lower shoreface marine and shoreface and nearshore marine lithofacies associations: (A) Hummocky

cross-stratification in fine-grained sandstone, offshore to lower shoreface marine lithofacies association. Pen for scale; Dead Horse Pass Formation, north-south-trending

ridge northwest of Dollar Lake, Henry’s Fork Basin. (B) Fine-grained sandstone to siltstone interbeds within the tabular quartzose lithofacies, upper shoreface and nearshore

facies association. Fine-grained sandstone to siltstone interbeds have an erosive upper contact and are overlain by medium-grained sandstone. Desiccation cracks are locally

present below such sandstone beds. Hammer for scale; Mount Agassiz Formation north of Gunsight Pass. (C) Decameter-scale, southward prograding inclined foresets of

shoreface sandbar (chenier of Wallace, 1972), tabular quartzose lithofacies upper shoreface and nearshore facies association. Circled bush is about 2 m long. Ledge outcrop

below north face of Kings Peak, Kings Peak quadrangle, Mount Agassiz Formation. (D) Laterally continuous tabular to swaley bedding, with occasional hummocks (Fig. 7A) in

fine-grained silty sandstone and interbedded dark mudstone, siltstone lithofacies, offshore to lower shoreface marine lithofacies association. Hammer for scale; basal Dead

Horse Pass Formation, north-south-trending ridge northwest of Dollar Lake, Henry’s Fork Basin. (E) Current rippled and flaser bedded sandstone overlain by parallel- and

wavy-laminated silty sandstone and siltstone, tabular quartzose lithofacies, upper shoreface and nearshore marine facies association, Mount Agassiz Formation. Field of view

is 15 cm high. Outcrop along south wall of Milk Lake ridge, Painters Basin, central Kings Peak quadrangle. (F) Sharp contact (sequence boundary b) between the lenticular

arkose lithofacies, deltaic facies association (below) and tabular quartzose lithofacies, upper shoreface and nearshore marine facies association (above: Island Lake quartzite

tongue of lower Red Castle Formation). Note the dramatic contrast between the immature, coarse-grained, arkose and the mature, well-sorted red-colored quartz arenite.

Map board, 12 in. high, for scale. Outcrop located along creek just west of the Red Castle. (G–L): deltaic and fluvial facies associations (G) Rhythmically stacked, tabular,

aggradational bedding geometry, tabular arkose lithofacies, deltaic facies association, middle Red Castle Formation. Cliff-wall outcrop is ∼305 m high. Located east of Henry’s

Fork river near Dollar Lake (within Fig. 2 photopanel). (H) Trough-cross bedding within crudely tabular medium beds, tabular arkose lithofacies, deltaic facies association,

middle Red Castle Formation. Note recessive intervals (finer-grained fraction) between tabular beds. Dog is ∼35 cm tall. Ledge outcrop below the east flank of Mount Powell

along the north-west wall of Henry’s Fork basin. (I) Mud draped reactivation surface (black arrow), tabular arkose lithofacies, deltaic facies association, upper Red Castle

Formation. Pencil for scale. Outcrop located along the eastern edge of Henry’s Fork basin north of Gunsight Pass. (J) Lenticular to wedgeform beds with accretion surfaces

(black arrows) and internal crossbedding, lenticular arkose lithofacies, deltaic facies association, lower Red Castle Formation. 1.5 m Jacob Staff (circled) for scale. Note lateral

accretion surfaces in middle of photo. Outcrop located in the western Mount Powell quadrangle south of Island Lake. (K) Intimately associated fine- and coarse-grained units,

tabular arkose lithofacies, deltaic facies association, upper Red Castle Formation. Note mud rip-up clast in upper left corner (with arrow), cm-scale interbedded siltstone and

coarse-grained arkose, and mud-draped foresets (dark colored inclined laminae). Hammer for scale. Outcrop located above Dollar Lake, east wall of Henry’s Fork Basin, Kings

Peak quadrangle. (L) Channel forms with poorly developed accretion surfaces and thin silty interbeds, lenticular quartzose lithofacies, fluvial facies association (formation of

Hades Pass). Field book and hammer for scale. Outcrop located along the east-trending claw-like ridge that separates Painter Basin (north) from Atwood Basin (south), along

Trail Rider Pass, Kings Peak quadrangle.

E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84 75

Fig. 7. (continued ).

tracts that stack to form depositional sequences that in turn stack hundreds of meters of strata (Fig. 5). Interpreted lithofacies associ-

to form a partial composite sequence (Fig. 5). ations include offshore to lower shoreface marine, upper shoreface

and nearshore marine, deltaic, and fluvial. These depositional envi-

5.1. Lithofacies and facies associations ronments are generally similar to those proposed by Wallace

(1972).

We broadly identify six lithofacies and four facies associations Unlike similar studies in Phanerozoic strata, the depositional

based on characteristic lithology/grain size, sedimentary struc- environment of Precambrian strata is difficult to determine due to

tures, bed geometry, and detrital zircon signatures within the Red an absence of diagnostic trace and body fossils. The increased ambi-

Castle, Dead Horse Pass, Mount Agassiz and Hades Pass forma- guity of paleoenvironmental interpretation of Proterozoic rocks

tions. We present photographs of representative lithofacies in Fig. 7, presents a unique challenge, offset in the UMG by spectacular

detailed lithofacies observations in Table 3, and interpretations in preservation of sedimentary structures. We rely on these sed-

the text, below, under the sub-header ‘interpretations’ within a imentary structures, facies architecture, the nature of contacts,

separate subsection for each facies association. and lateral-vertical facies changes to interpret depositional envi-

Lithofacies are resolved on a meter to tens-of-meter scale with ronment. We recognize the particular ambiguity of fine-grained

the goal of capturing the lateral and vertical facies changes through deposits, which can lack physical sedimentological information.

76 E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84

5.1.1. Offshore to lower shoreface marine facies association deposition. Textural and compositional maturity, cross bedding,

(mudstone and siltstone lithofacies) mudcrack casts and local scouring into mudstone units below

Observations: Refer to Table 3. (Fig. 7b) indicate the tabular quartzose lithofacies was deposited

Interpretation: The mudstone and the siltstone lithofacies under moderate to high energy, under shallow to subaerial con-

(Fig. 7a and d) record the most distal marine environments in ditions, and characterized by significant sediment reworking. The

the middle UMG. Decimeter- to meter-thick accumulations of gross upward-fining trend over greater than 100 m from the Dead

parallel-laminated black to green clay-shale (mudstone lithofa- Horse Pass to Mount Agassiz formations, flaser beds (Fig. 7e) and

cies) record a low-energy environment mainly below storm wave occasional mud cracks suggest a transition up section to deposition

base. Centimeter-thick, fine-grained, wavy-laminated sandstone within a shallow, low-energy environment, perhaps a back barrier

beds represent storm-derived fluxes of coarser-grained material lagoon or an estuary, near the bedload convergence zone under

deposited near storm wave base (Fig. 7d). Fine-grained sandstone mixed marine and fluvial processes (Dalrymple and Choi, 2007).

and siltstone with hummocky cross stratification and plane beds

(siltstone lithofacies, Fig. 7a) record deposition above storm wave

5.1.3. Vertical facies transition between the offshore to lower

base in the offshore-transition zone of a wave-affected shoreline

shoreface marine facies association and the upper shoreface to

(Dumas et al., 2005; Dumas and Arnott, 2006; Dalrymple and Choi,

nearshore marine facies association

2007). Microfossils in the mudstone lithofacies (unpublished data,

The mudstone and siltstone lithofacies (offshore to lower

Kingsbury, 2008) are similar to those found in other fine-grained

shoreface marine facies association) and tabular quartzose lithofa-

UMG sediments (Dehler et al., 2005) and are interpreted to indicate

cies (upper shoreface to nearshore marine facies association) form

deposition below a shallow chemocline in an intracratonic seaway,

decameter- thick, upward-coarsening cycles with sharp, often ero-

similar to the Black Sea today (Nagy and Porter, 2005; Nagy et al.,

sive upper and lower contacts. The lower contact of each cycle is

2009).

overlain by the mudstone or the siltstone lithofacies (Fig. 7a and d,

Figs. 2 and 5), which grades into the tabular quartzose lithofacies

(Table 3, Figs. 2 and 7c and e).

5.1.2. Upper shoreface and nearshore marine facies association

(tabular quartzose lithofacies)

Observations: Refer to Table 3. 5.1.4. Deltaic facies association (tabular and lenticular arkose

Interpretation: The tabular quartzose lithofacies is interpreted to lithofacies)

represent upper shoreface and nearshore marine deposits within Observations: Refer to Table 3. The lateral expression of the

several upward-coarsening stratigraphic successions that record deltaic facies association varies from west to east across the study

offshore-transition through upper shoreface/nearshore marine area (Fig. 5). The lenticular arkose lithofacies (Fig. 7f,j) is only

Fig. 8. Photopanel of the northwest-facing (Fig. 8A) and north-facing (Fig. 8B) ridges of Gilbert Peak above Gilbert Lake, the reference section for the Dead Horse Pass and

Mount Agassiz Formations. The box indicates the area of the zoomed-in photos. The arrow points to the northwest. Close up of strata, with interpreted stratal geometry

shown in the lower photos. DS = Depositional sequence. Zuc: Red Castle Formation; Zud: Dead Horse Pass Formation; Zuma: Mount Agassiz Formation.; Zuh: formation of

Hades Pass.

E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84 77

Fig. 8. (continued ).

exposed in the western study area (Mount Powell quadrangle, south-directed paleocurrents, and soft-sediment deformation)

Fig. 1) and may be present in the subsurface of the eastern study suggest a proximal, northern source and rapid deposition of

area (Kings Peak quadrangle, Fig. 1). The tabular arkose lithofacies upward-fining bodies of sediment. Tidal influence is locally sug-

(Fig. 7g–k) is exposed in both quadrangles. To the west (Mount Pow- gested by bi-directional north- and south-trending paleocurrents

ell quadrangle) it is coarser-grained with south-directed paleoflow and ubiquitous, intimately associated fine- and coarse-grained

(Figs. 5 and 7h) and locally contains decameter-scale, south- material on a millimeter- (mud-draped foresets, Fig. 7i) to

dipping low-angle foresets. Paleoflow is to the north in the eastern decameter-scale (interlayered mudstone, siltstone, and tabular

study area. Although mudstone lithofacies interbeds are more arkose lithofacies, Fig. 7g), which indicate repeated fluctuation

frequent up section across the study area, mudstone lithofacies between suspension-fallout and bedload movement processes.

interbeds are thickest and most abundant to the east (Kings Peak These strata are comparable to other tidally influenced deposits

quadrangle, Fig. 7g). (e.g., Clifton and Phillips, 1980; Fedo and Cooper, 1990; Dalrymple,

Interpretation: We interpret the deltaic facies association to 1992; Brettle et al., 2002), including the correlative Big Cottonwood

represent a tidally influenced braid-delta fed by a south-flowing Formation (Ehlers and Chan, 1999; Dehler et al., 2010).

fluvial system that was transverse to the larger, east-west trending Channelforms with internal cross-bedding, common mud rip-

shallow marine depositional environment. Fig. 11 is a schematic up clasts, coarse, euhedral feldspar grains, and occasional siltstone

environment of deposition map meant to illustrate facies rela- caps characteristic of the lenticular arkose lithofacies suggest depo-

tionships through time for the middle UMG within the study sition of braid bars within braided distributary channels on a

area. Textural and compositional immaturity, detrital zircons proximal delta plain Fig. 11a). Common tabular quartzose litho-

and sedimentary structures (e.g., climbing ripples and dunes, facies interbeds record interaction between the braid delta and

78 E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84

the marine body it opened into and indicate fluctuations between and Phillips, 1980; Dalrymple et al., 1992; Dalrymple and Choi,

shoreface to nearshore marine or fluvial processes (Fig. 11b and c). 2007).

Cross-stratification and km-scale, laterally consistent tabular

bed geometry, overall finer grain size and greater textural matu-

rity (as compared to the lenticular arkose lithofacies) characteristic 5.1.5. Fluvial facies association (lenticular quartzose lithofacies)

of the tabular arkose lithofacies suggest sheets of subaqueous Observations: Refer to Table 3.

dunes traveling across a broad, well-developed delta plain (Fig. 7g, Interpretation: Following Wallace (1972), the lenticular quart-

Long, 1982; Miall, 1984, 1992, 1996; Yoshida, 2000). Interbeds zose lithofacies (Fig. 7l) records braided fluvial deposition as

of the offshore marine facies association indicate delta front suggested from stacked, lenticular-shaped, upward-fining beds,

deposition. sedimentary structures, and paleoflow. Stacked, lenticular bed

Proximal delta plain deposits dominated by fluvial processes geometries with erosive bases (channel forms) and siltstone caps

transition to medial/distal delta plain to delta front deposits record braid bar deposition (Miall, 1984, 1996). The high sand to

dominated by tidal processes from the west (Mount Powell siltstone ratio supports braided fluvial deposition, where overbank

quadrangle) to east (Kings Peak quadrangle) across the study deposits are poorly developed and often cannibalized by braided

area (Figs. 1, 5 and 11). Coarser-grained sediment, channelform river channels. Braided fluvial systems were likely common in the

bed geometries, and south-directed paleoflow observed in the Proterozoic due to decreased bank stability and increased sedimen-

Mount Powell quadrangle record a south-flowing fluvial system tation rates caused by an absence of terrestrial plant life (Long,

(Fig. 11a). Finer-grained sediments, increased frequency of offshore 1982). Fluvial braid plains are identified in other ancient marine

marine facies association interbeds, and primarily north-directed through tidal estuarine to fluvial depositional systems (e.g., Fedo

paleoflow to the east (Kings Peak quadrangle, Figs. 1 and 5) and Cooper, 1990; Yoshida, 2000). The gradation from lenticular

record an eastward transition to a delta front to prodelta envi- quartzose to lenticular arkose lithofacies from east (Kings Peak

ronment (Fig. 11c). North-directed paleocurrents record sand quadrangle) to west (Mount Powell quadrangle) demonstrates

deposition during dominant flood tides. Similar flood tide deposits the persistence of the Red Castle river system throughout UMG

are observed in other ancient and modern deposits (e.g. Clifton deposition.

Fig. 9. Photopanel of the east-facing wall of Kings Peak above Painter Basin. The box indicates the area of the zoomed-in photos. The arrow points towards north. A shows

stratal geometry on the north end of this ridge. (B) shows stratal geometry on the middle southern part of the ridge. Close up of strata, with interpreted stratal geometry

shown in the lower photos. DS = Depositional sequence. Zuma: Mount Agassiz Formation; Zuh: formation of Hades Pass.

E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84 79

Fig. 9. (continued ).

5.2. Vertical stacking patterns 4 through 6 stack with a gross upward-shallowing trend from

offshore marine (siltstone lithofacies, upper member, Red Castle

Eight depositional sequences stack to form one nearly complete Formation) through upper shoreface/nearshore marine (tabular

composite sequence within the study area. Depositional sequences quartzose lithofacies, upper member, Red Castle Formation) to

1 through 3 each shallow upward from upper shoreface/nearshore tidally influenced deltaic distributary channel bars (tabular arkose

marine deposits (tabular quartzose lithofacies) to tidally influ- lithofacies, upper member, Red Castle Formation). To the west,

enced, deltaic distributary braid bars (lenticular and tabular arkose the increase up-section of the tabular arkose lithofacies is inter-

lithofacies). Depositional sequences thicken, and the tabular arkose preted to record progradation of a mature, broad, relatively

lithofacies is predominant, up-section and especially within depo- flat braid plain (Fig. 5). In the Kings Peak quadrangle deposi-

sitional sequence 3 (Fig. 5). tional sequences 4 through 8 each shallow upward from offshore

Depositional sequences 4 through 6 each shallow upward marine (siltstone and mudstone lithofacies, lowermost Dead Horse

from offshore marine through shoreface/nearshore marine and/or Pass Formation) to upper shoreface/nearshore marine (tabular

deltaic facies associations. The deltaic facies association is predom- quartzose lithofacies, Dead Horse Pass and Mount Agassiz for-

inant to the west while marine facies associations are predominant mations). Depositional sequences 6 through 8 are aggradationally

to the east. In the Mount Powell quadrangle depositional sequences and possibly progradationally stacked and contain offshore and

Fig. 10. Photopanel of cirque at head of Smiths Fork west of the Red Castle. The arrow points towards west. Upper photo shows strata without interpretation, lower photo

shows interpreted stratal geometry. Movement symbols next to arrows indicate onlapping and downlapping at an angle to the cliff face, with some component of movement

into and out of the page (to the north or south) and some component of movement along the strike of the page (to the east or west). A circled x indicates the strata is

downlapping to the south (into the page) and west (along the strike of the page to the right). DS = Depositional sequence; Zucm = middle Red Castle Formation; Zucu = upper

Red Castle Formation.

80 E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84

Fig. 11. Schematic reconstruction of depositional environments for the middle Uinta Mountain Group exposed in the study area (Red Castle to Mount Agassiz formations

and the formation of Hades Pass). An east-west-trending shoreline is fed by a south-flowing braided fluvial system and a west-flowing braided fluvial system. The location

and significance of the depositional environments depicted in this figure fluctuated throughout the evolution of the UMG basin, as reflected in the sequence stratigraphic

interpretation presented herein. For example, at the time of deposition of the formation of Hades Pass, the west-flowing fluvial system prograded out across the entire study

area above composite sequence boundary 2 (see Fig. 5) Lettered rectangles represent the approximate locations of the Mount Powell and Kings Peak quadrangles within this

depositional environment as it evolved through time, during the deposition of the (A) lower Red Castle Formation (exposed in the Mount Powell quadrangle, may be present

in the subsurface of the Kings Peak quadrangle); (B) middle Red Castle Formation and Dead Horse Pass Formation; (C) upper Red Castle and Mount Agassiz Formation and

(D) formation of Hades Pass.

upper shoreface to nearshore marine including fine-grained, low the offshore to lower shoreface facies association (Fig. 5e, Fig. 12).

energy, shallow water, perhaps back-barrier estuarine or lagoon These fine-grained strata in turn coarsen upwards into offlapping

deposits. quartz arenite of the upper shoreface and nearshore facies asso-

ciation. The uppermost quartz arenite strata are truncated by an

5.3. Stratal geometries, terminations, and surfaces upper, erosive boundary of depositional sequence 4.

We interpret the lower, erosive boundary of depositional

Significant surfaces are identified by an abrupt facies change, sequence 4 as a composite transgressive surface (CTS1). Detrital zir-

stratal geometries, and stratal terminations (onlap, downlap, and cons in the siltstone lithofacies (offshore to lower shoreface marine

truncation). Sequence boundaries truncate underlying strata with facies association) (Fig. 6c) at the base of depositional sequence

up to several meters of erosional relief, frequently pass laterally into 4, immediately above CTS1, contain a dominant Archean detrital

their correlative conformities (Catuneanu, 2006) and are frequently zircon age peak. The Archean age peak indicates reworking of the

overlain by onlapping offshore marine facies (Fig. 2). underlying tabular arkose lithofacies and suggests significant scour

A composite sequence boundary (CSB 3, contact between the associated with marine transgression occurred across CTS 1.

Mount Agassiz or upper Red Castle and the Hades Pass formations, As can be seen in Fig. 12, a retrogradational systems tract

Fig. 5) can be mapped for tens of kilometers in the central Uinta (RST, sensu Neal and Abreu, 2009; traditional terminology: trans-

Mountains. It is exposed on the east wall of Kings Peak (Fig. 9) and gressive systems tract, sensu Mitchum and Van Wagoner, 1991),

northwest of the Red Castle (Fig. 10) where a basinward shift from composed of onlapping offshore through nearshore and shoreface

offshore and shoreface marine to braided fluvial facies is observed marine lithofacies, overlies CTS1 and forms the base of deposi-

across the sequence boundary. Composite sequence boundary 3 tional sequence 4. A maximum flooding surface is likely present

cuts out the upper half of depositional sequence 8 at Gilbert Peak within the fine-grained strata that make up the middle part of the

and Milk Lake (Fig. 5e and f). It cuts down section from east to west, sequence. An aggradational–progradational systems tract, (APST;

eliminating depositional sequences 7 and 8 near the Red Castle

(Fig. 5b and c).

We highlight depositional sequence 4 (Fig. 12), exposed on the

northwest flank of Gilbert Peak, to explain how we identify deposi-

tional sequences across the study area. Depositional sequence 4 is

bounded below by an erosive surface that truncates several meters

of underlying tabular arkose lithofacies (deltaic facies association)

and is overlain by onlapping strata of the offshore through upper

shoreface and nearshore marine lithofacies association (Fig. 2,

lower left, Fig. 5e, Fig. 12). Swaley-bedded fine-grained sandstone,

siltstone, and interbedded shale are present immediately above

the basal erosive surface. Interbedded, swaley, hummocky cross-

bedded, and plane-bedded, fine-grained sandstone, siltstone, and

shale are present above the same stratigraphic horizon several kilo-

meters to the west, at Dollar Lake (Fig. 7a and d, Fig. 5d). Quartz

Fig. 12. Close up view of depositional sequence 4, northwest face of Gilbert Peak,

arenite of the upper shoreface and nearshore marine facies asso-

Kings Peak quadrangle. Vertical exaggeration is 30 to 1. The view shown in this figure

ciation fines upward into several meters of shale and siltstone of is enlarged from Fig. 8A.

E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84 81

detrital zircon provenance, frames the middle UMG within a pre-

dictive stratigraphic hierarchy (sensu Neal and Abreu, 2009). Our

documentation of tidal marine and fluvial-deltaic depositional

environments is consistent with tidal interpretations for the correl-

ative Big Cottonwood Formation of the Wasatch Range (Chan et al.,

1994; Ehlers et al., 1997; Ehlers and Chan, 1999) and demonstrates

that this mid-Neoproterozoic (∼770–740 Ma) epicontinental sea-

way was connected to the world ocean (Panthalassa). Broadly

coeval marine strata to the south include the Chuar Group of the

Grand Canyon and the middle Pahrump Supergroup of the Death

Valley area (Fig. 13, Mahon et al., 2012). The existence of a signif-

icant Rodinian epicontinental seaway implies the future western

margin of Laurentia was affected by faulting and long-term (>30 Ma

duration) subsidence even before it became a west-facing passive

margin.

Sequence Stratigraphy of the Uinta Mountain Group records

the interface between this epicontinental sea, local south-

draining, coarse-grained fluvial systems, and a major west-draining

Fig. 13. 770–740 Ma Rodinian paleotectonic reconstruction (after Goodge et al.,

transcontinental river system and reveals potential controls

2008 and Foster et al., 2006) showing Uinta Mountain Group half-graben extend-

on stratal packages. The eight higher-frequency depositional

ing west to include Big Cottonwood and Little Willow formations. The Chuar

Group and upper Pahrump Group were deposited in the same intracratonic sea- sequences may be driven by shorter-term autocyclic and allo-

way. The south-flowing Red Castle River drains Neoarchean Wyoming Province.

cyclic events, including delta lobe switching, avulsions, climatic

The west-flowing Laurentian big river drains Proterozoic Yavapai, Mazatzal, and

fluctuations and local tectonism, whereas the composite sequence

Trans-Hudson provinces as well as Grenville orogenic belt.

records the longer-term transgression of the epicontinental sea.The

absence of well-developed lowstand systems tracts within the

traditional terminology: highstand systems tract) composed of

study area may be explained by a combination of the overall,

downlapping quartz arenite of the upper shoreface and nearshore

longer-scale retrogradational trend of the system and the hypoth-

marine facies association, overlies the maximum flooding surface,

esized large lateral extent (tens to hundreds of kilometers) of

and forms the upper part of depositional sequence 4. The upper-

lithofacies across the broad, low-gradient basin floor of the epi-

most strata of the aggradational–progradational systems tract are

continental sea. Lowstand systems tracts may have developed in

truncated by an erosive surface that forms the upper sequence

more distal locations beyond the study area.

boundary of depositional sequence 4.

Longer-term Neoproterozoic eustatic sea level rise was likely

driven by breakup of the supercontinent Rodinia (Li et al., 2003,

5.4. Sequence stratigraphic interpretation 2008; Zhu et al., 2011). Plate reorganization is recognized as a driver

for sea level change: Generation of new, hotter and more buoyant,

Depositional sequences stack to form a progradational– sea floor material decreases ocean basin volume, causing marine

aggradational sequence set (PASS, sensu Neal and Abreu, 2009) transgression (Heller et al., 1996). Shorter-term drivers on Neopro-

and an aggradational–progradational sequence set (APSS). In tradi- terozoic cyclcity are poorly constrained, although glacioeustacy has

tional sequence stratigraphic terminology these would be labeled been suggested as a control on coeval deposits (Dehler et al., 2001a;

“lowstand” and “highstand” sequence sets (Mitchum and Van Mahon et al., 2012).

Wagoner, 1991). Each depositional sequence is comprised of Given available geochronology, the most likely candidate to

a basal, relatively thin, retrogradational systems tract (RST, or drive long-term eustatic transgression at 770–740 Ma was east

“transgressive systems tract”), represented by onlapping fine- Asian rifting. Basalt and dacite-rhyolite of the Beiyixi volcanics

grained strata, and an upper, relatively thicker, aggradational– within the Tarim block (northwest China) are interpreted as recor-

progradational systems tract (APST), represented by aggradational ding continental rift-related magmatism and are dated by U–Pb

to downlapping sandy strata. A composite transgressive surface using SHRIMP at 755 ± 15 Ma (Xu et al., 2005). Granitoids and mafic

(CTS 1, Fig. 5) separates the lower PASS from the upper APSS to ultramafic rocks of the Chengjiang magmatics within the Yangtze

(Figs. 2, 8 and 10). Sequence sets stack to form one nearly com- Craton (South China) are interpreted as syn-rift magmatics and are

plete composite sequence (CS2, Figs. 3 and 5) bounded above by a dated by U-Pb using SHRIMP with ages ranging from 775 ± 8 to

mappable composite sequence boundary (CSB3 on Fig. 5). 751 ± 10 Ma (Li et al., 2003, see also Lin et al., 2007; Li et al., 2008).

This rift episode corresponds with the second of three magmatic

6. Discussion pulses recognized in the Tarim block between ca. 790 and 740 Ma

by Zhu et al. (2011). The youngest magmatic pulse within Tarim was

The Uinta Mountain Group can now be better understood in its 650–615 Ma and suggests that rifting of Rodinia was a long-lasting

regional paleogeographic context of a mid-Neoproterozoic epicon- process. A multi-stage rift argument is supported by 705–667 Ma

tinental sea that covered western Laurentia at least 150 million volcanic ages from Idaho and Utah (Keeley et al., 2013; Balgord

years before the inception of the Cordilleran passive margin at et al., 2013).

600–550 Ma (Fig. 13) (Wallace, 1972; Dehler et al., 2010; Link We do not favor the paleocontinental reconstruction of Li et al.

and Christie-Blick, 2011). The recognition (Dehler et al., 2010; this (2008), which places South China adjacent to southern Lauren-

study) of marine (specifically tidal) lithofacies and shallow-marine tia, but we recognize the importance of supercontinental breakup

sequence stratigraphic stacking patterns invalidates the interpre- as a driver for transgression of the Chuar-Uinta Mountain Group-

tation of the UMG as a lacustrine system analogous to the cyclic and Pahrump Group seaway. The generation of new oceanic lithosphere

persistently aggradational Belt Supergroup of southwest Montana during supercontinental rifting is recognized as a major forc-

(e.g. Link, 1993; Winston and Link, 1993). ing mechanism for long-term (several millions of years) eustatic

The identification of tidal marine and fluvial-deltaic depo- sea level change (e.g. Cogne and Humler, 2008; Heller et al.,

sitional sequences based on physical surfaces, lithofacies, and 1996).

82 E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84

We favor the reconstruction of Goodge et al. (2008), which 780 Ma, and ‘zipper rifting’ of Laurentia starting at ca. 750 Ma,

places Antarctica and Australia as the western continents that even- most likely drove long-term eustatic transgression at 770–740 Ma.

tually rifted from Laurentia (Fig. 13). This reconstruction correlates Drivers for nested depositional sequences 1 through 8 reflect a

distinctive 1400 Ma granites in East Antarctica to similar plutons of combination of higher frequency autocyclic and allocyclic con-

the mid-continent A-type granites of southern Laurentia. Further trols. Further investigation of the lateral correlation of sequences

it allows for 1490–1610 Ma detrital zircon grains sourced in the and sequence sets, and improved time constraints, will clarify the

Gawler Volcanics of South Australia to be deposited in the 1450 Ma importance of autocyclic (delta lobe switching, channel avulsion)

lower Belt Supergroup of Idaho and Montana (Ross and Villeneuve, and allocyclic (regional tectonism, climatic fluctuations) controls

2003; Link et al., 2007). Paleomagnetic studies from the UMG, Chuar on UMG deposition. A refined understanding of controls on UMG

Group, and the 720 Ma Franklin Dike Swarm of northern Lauren- higher-frequency depositional sequences is significant towards

tia indicate an equatorial paleolatitude for the UMG epicontinental unraveling Neoproterozoic climate fluctuations prior to the onset

sea within this larger paleogeographic setting (Fig. 13) (Weil et al., of the first phase of low-latitude Sturtian glaciations.

2004, 2006; Evans and Raub, 2011). The Neoproterozoic western Two detrital-zircon signatures are recognized in the UMG. One

Laurentian epicontinental seaway can be used as a tie-point with signature has a well-defined Neoarchean peak, and one signature

other continents to further constrain the original continental con- has mixed Proterozoic and Archean age components. Lithofacies

figuration of Rodinia. with a Neoarchan detrital zircon signature were transported by a

In addition to east Asian rifting, rifting in northern Laurentia local south-flowing river system draining the southern Wyoming

(present coordinates) likely also contributed to eustatic sea level province, or reflect significant transgressive marine ravinement

rise. Onset of rifting that produced northern Laurentian oceanic across a composite transgressive surface (CTS 1) that eroded and

crust may have propagated southward, starting in the Canadian reworked deposits from this transverse river system. Lithofa-

Cordillera at 750 Ma (“zipper-rift”, Eyles and Januszczak, 2004). This cies with a mixed detrital zircon signature were transported and

rift phase is closest in space, and overlapping in time, with half- deposited by a major, west-flowing river system with a drainage

graben subsidence of the UMG basin. Crustal thinning expressed as basin that included much of Laurentia, or were deposited under

750 Ma continental rifting in the western Canadian Cordillera may dominantly marine processes that mixed and reworked these sed-

have been a distal cause for the regional faulting and subsidence of iments.

the UMG basin. Neoproterozoic anorogenic magmatism is recorded Documentation of tidal marine and fluvial-deltaic depositional

in the mafic Gunbarrel dike swarm event in western Laurentia, as sequences within the UMG is consistent with previous tidal

far south as the Teton Range in northwest Wyoming (780.3 ± 1.4 interpretations for the correlative Big Cottonwood Formation of

U–Pb baddeleyite analyses, Harlan et al., 2003). Although the north- the Wasatch Range and requires that this mid-Neoproterozoic

∼

ern American Cordillera appears to have rifted at 750 Ma (Colpron ( 770–740 Ma) intracontinental seaway was connected to the

et al., 2002), there is no evidence of rift-related magmatism south world ocean. Thus, we conclude that continental breakup of

of the Gunbarrel dikes until after 720 Ma (Harlan et al., 2003; Lund, southwestern Laurentia was episodic and fitful, starting with for-

2008; Balgord et al., 2013). In the Pocatello Formation of southeast mation of the Uinta Mountain Group-Big Cottonwood Formation

Idaho, the age of rift-related mafic and trachytic volcanism is ca. half-graben at ∼750 Ma. Mafic volcanism and glacial marine sed-

717–685 Ma (Keeley et al., 2013). imentation of the Pocatello and Perry Canyon formations lasted

Likely controls on the eight higher-frequency depositional from 717 to 685 Ma (Fanning and Link, 2004; Keeley et al.,

sequences are autocyclic (delta avulsion, tidal channel migration) 2013). Development of the carbonate passive margin did not occur

and allocyclic (episodic tectonism, climate fluctuations). Similar m- until after 550 Ma (Link and Christie-Blick, 2011; Balgord et al.,

scale and 100-m scale shallowing-upward cycles are present within 2013).

the coeval Chuar Group (Grand Canyon; where Dehler et al., 2001a

inferred a glacioeustatic control), and in the middle Pahrump Group

(Death Valley) (Mahon et al., 2012). A regional understanding of the Acknowledgements

lateral nature (directional thinning; lateral extent) of sequences

and sequence sets and better time constraints are required to This work summarizes the M.S. theses of Kingsbury (2008)

understand the relative importance of autocyclic and allocyclic and Osterhout (2011). Support for this research was provided by

controls on UMG deposition. Future work on UMG epicontinental the U.S. Geological Survey, National Cooperative Geologic Map-

deposits may further constrain Neoproterozoic climate fluctuations ping Program Awards No. 07HQAG0145 and 10HQPA0004, to

prior to the onset of the first phase (716.5 Ma) of low-latitude Stur- Paul K. Link; National Science Foundation grant EAR-0819759 to

tian glaciations (Macdonald et al., 2010; Keeley et al., 2013). Link and Dehler; the Utah Geological Survey Mapping Division;

and the Idaho State University Graduate Student Research and

Scholarship Committee (FY07-R8). This manuscript benefited from

7. Conclusions review by Jeff Geslin at ExxonMobil Upstream Research Company,

Doug Sprinkel at the Utah Geological Survey, and an anony-

Facies and stratal architecture of middle Uinta Mountain mous reviewer. The Ashley National Forest and Luke Osterhout

Group strata in the central Uinta Mountains indicate offshore and provided field assistance. Diana Boyack helped greatly with the fig-

shoreface (lower and upper) and nearshore marine, deltaic, and ures. We also acknowledge the hospitality of George Gehrels and

fluvial facies associations organized into depositional sequences. University of Arizona Laserchron Lab for detrital zircon analyses

Eight depositional sequences are stacked within a lower-frequency, and Mark Schmitz at Boise State University for help with zircon

composite sequence that is composed of a progradational to aggra- separations.

dational (PASS; traditional terminology: “lowstand”) sequence set

overlain by an aggradational–progradational (APSS; traditional ter-

minology: “highstand”) sequence set. This composite sequence is Appendix A. Supplementary data

the middle of three composite depositional sequences in the UMG

that together reflect long-term eustatic sea level rise driven by Supplementary material related to this article can be found,

breakup of the supercontinent Rodinia. Rifting of the Tarim and in the online version, at http://dx.doi.org/10.1016/j.precamres.

South China blocks from Asian parts of Rodinia starting around 2013.06.015.

E.M. Kingsbury-Stewart et al. / Precambrian Research 236 (2013) 65–84 83

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