This article isprotected rights by All copyright. reserved. 10.1002/dep2. doi: lead todifferences version between this andthe ofPleasec Version Record. been and throughtypesetting, proofreadingwhich may thecopyediting, process, pagination This article undergone has for and buthas accepted been not review publication fullpeer o base traceable flooding and ravinement surfaces. The subsequent transgression, which defines the deformation episodes, resulted in lower Curtis wasdeposited A dominated by amplified tidal forces, resulting in a complex distribution of heterolithic deposits. from ( deposited. Wave energy wasefficiently dissipated by the shallow basin’s elongated morphology thewell as fluvial input throughout this basin, in which theinformal lower, middle, and upper Curtis, as modern Idaho Trough foreland basin and related sedimentary units in the environments, including Modern, tide ABSTRACT Correspondi Kingdom 3 2 1 STUART M. CLARKE VALENTIN ZUCHUAT EAST EPICONTINENTAL OVERPRINT typeArticle : Original Research Article MR. THOMAS J.H. DODD (Orcid :ID 0000 MR. VALENTIN ZUCHUAT (Orcid :ID 0000 British Geological Survey, theLyell Centre, Research Avenue South, Edinburgh, EH14 4AP, United Basin Dynamics Research Group, Tectonostratigraphic Research Group, approximately Acceptedllocyclic Article significant f the middle Curtis, -

CENTRAL UTAH systems. Persistent causedaridity the characteristic severe starvation ofperennial

forcing strongly

underlying Entrada Sandstone, and the ng author: [email protected] -

dominated and

800x1 wave impact ED 69 2 ALLOCYCLIC , 1

O , 5 ARVE R.N. SLEVELAND LE RABBEL 0 km), as its

deltas, estuaries, and lagoons. However, some tide BASIN: allowed impacted impacted . Short

. Consequently, the semi of t tide , USA he he - Keele University, Keele, Staffordshire,

-

influenced coastlines the accumulation of for the shallo lived relative sea 1 Jurassic THE UPPER , semi

upon the system’s intrinsic autocyclic processes

ALVAR BRAATHEN rock record, such as the semi

University of PROCESSES -

- 0003 enclosed - Curtis 0002 1 - , ROSS 2257 w - - 2029 marine part of thesystem to enter into tidal

sea overlying morphology Oslo, Sem Sælands Vei 03711, Oslo -

JURASSIC CURTIS FORM level variations, - - 6740) , donot correspond to any ofthese

enclosed P.

three parasequences, BY - are characterised by a range of 6422) 1 PETTIGREW ,

and

TIDAL RESONANCE

Summerville For

IVAR MIDTKANDAL , shallow

further protected - enclosed, shallow, Utah

along with 2 ST5 5BG, , THOMAS J.H. DODD - marine system was - dominated basins each mation were ite this ite this United Kingdom

uplift uplift and separated by the 1

ATION, as the , Norway

article as system IN

A - 2 / N 3 ,

This article isprotected rights by All copyright. reserved. approximates forces,tidal Sea, 2018). comparatively small variations in water depth (Midtkandal uponplace a low interpretation of the deposits ofa tide the rate 1991), such as pattern Wang, 2012; transport S channeltidal dispersal of distribution dimensional S the land, or whether forming as portion of the sea?” (translation from Bostock overflowing waves ofthe ocean”, leaving wonder if they to“are be looked upon belonginas century AD, when Pliny the Elderdescribed areas “invaded twice each day and night by the (Kvale, 2012) Oceanic tides INTRO stratigraphic surfaces, Keyword auto understand relationships ofneighbouring and contemporaneous depositional systems that allocyclic processes by autocyclic behaviour. optimal morphological configuration, leading to the overprinting ofotherwise dominant This showsstudy that a tide the Curtis the as Moab Member However, the contemporaneous and neighbouring overprinted wavelength approximately 800 resonance Acceptedpatio edimentary succession Article the Persian Gulf, orthe Bay of Fundy, cyclic - supratidal deposits

In addition, modern temporal s

DUCTION and frequency

of sedimentation - s

sea sea deposition chain, further and allocyclic processes as a consequence of

A ing ofthe

given an average minimum water depth of20to 25 m allowing basinal hydrodynamic forces

of which the effects eolian sequences, allocyclic processes, ( s Baas

. 3D and their spatio , and

regressed. to

The variations of the Curtis Formation

) variations tidal of currents, - an odd multiple , gradient and slope

et al.

complex environments they uponact have raised people’s interest early as first

(iii) km in length

the system to enter a tidal resonant stagetheif length of the basin dynamic stratigraphic history ofa alternativelybasin dominated by depends on a fine balance

t

, 2016) at which the of allocyclic forcing and related traceable stratigraphic surfaces. sediment i idal resonance s

deposited within tide in , of the

are ultimately governed by allocyclicly driven phenomena (Osleger,

- and potentially cyclic day, - relative searelative dominated basin can enter into - . temporal

the These intrinsic and interacting processes

, Summerville Formation s

corresponding to an odd multiple of thequarter of emi nput (Kvale, 2012; Wang, 2012

flooded can can be y complicate the arrangement of a

facies belts are shifted over large horizontal distances by - occur (Strasser quarter of the wavelengthtidal enclosed basins - . ,

dominated basin, sediment deposition typically takes characterised by five stacked aeolian sequences - variability level ,

achieved demonstrate thatbasin geometry (ii) basin reach

which It is It is only by considering the

and autogenic - dominated basin between

assemblage

changes in

coastal dune field s . are complex and dynamic

variably

autocyclic processes, et al. , such as the Gulf of California, the Adriatic ing basin , lingered to record allocyclic signals, as

(i) (i) basin configuration and

, 1999). To complicate the optimal configuration

& influenc tidal

available accommodation, and by

of heterolithic lithologies Nystuen, 2009 processes s , resonance itreachesas its

. resonantThis system and are characterised by these deposits e

(Sz

the

ediment references therein). , such as tan ,

Curtis Formation sedimentological and system’s ó can ;

& phenomena Zuchuat their their ary rocks &

de Boer, 1995; a further further

further

Riley, Riley, 1855) the avulsion of full full

. of the tidal (Kvale, 2012; erosion associated

of the et al. , a three

, as well the

amplify of the the

-

, , g to .

-

This article isprotected rights by All copyright. reserved. level high identifies contemporaneous shallow insights (C aeolian to develops Zuchuat Jurassic Curtis This setting environment east The sedimentary record, especially when sediments within them embayments (Zuchua epicontinental basins evidence oftidal reworking corresponds to Harris dominated deltas, transg shallow Notwithstanding sequestration projects reservoir sediments are tidally dominated sedimentary successions typically host Despite a complicated resonant at different time sediments resonance is geologically D rise transgressive setting The impact of such Longhitano Boer’s, 1995; Yoshida stronger tidal currents Dalrymple, 2012; Shaw Martinius alrymple, 2012 Acceptedaputo Article often - (Sztan continuous and - study study central frequency ( Boulila ressive, upward et al. through - into & water, et al.

that framework laterally and vertically sealed targets key sequence stratigraphic

&

. Consequently, a ó Pryor, 1991; Peterson, 1994; Doelling, 2001; Zuchuat can be provides a detailed analysis , 2002;

et al. shallow Gowland, 2011; Roos

Utah & the behaviour of neighbouring aeolian deposits and their relationships to the

’s that et al.

de Boer’s, 1995 and Summerville

(2018) tide systemic responses to varying climat time , 2012; Reynaud ; references therein

for the inherent complexities ofsediment character and distribution,

(Fig. short, compound, and evolves or

, 2010 Fan, 2012) - autocyclic - dominated three . marine the s

(iv) open

t , as (Tape et al -

and 2

lower, middle, and upper Curtis et al. (Martinius , fining estuari closer to the shoreline than in open water

et al. ) but a hydrocarbon , 2011

allows instantaneous, the system’s resonance s further tofurther r the into dimensional

. -

spatio , 2007; (Reynaud marine and paralic realm , 2018)

basin et al. , 2014)

se sedimentary systems

lack of lack modern day equivalent . processes has been detected ; Martinius

- a semi However, not every sedimentary ; , coast tidal flat

coastal Alberti detailed investigations of formations - , 2003; Zuchuat & . assessmentThe of theMoab Member ofthe Curtis Formation temporally & et al. Martinius

may may display Dalrymple, 2012; .

Schuttelaars, 2011; Longhitano ) es, (ii) (semi A consequence ofthis

econstruct the kinematic history of - . surfaces 3D & enclosed, fluvially exploration However,

, 2005; Halland exposure ofthe

of by et al. depositional systems Dalrymple, 2012) spatially

and the continuous exposure is

& the finer grained,finer low porosity and low permeability

Gowland, 2011; one (Wilcox , &

2012; compartmentalised Middle Jurassic Entrada Sandstone , such floodingas surfaces, (Fig. 1

Gowland, 2011;

of these four strong evidencefor tidal rework the time interval - et al. variable typically increases

) industry

protected lagoons, (iii) prograding, tide Strasser ; time & . e Boyd

Shaw Shaw The have , 2018

conditions Currie, 2008) et al. middle to upper Jurassic lithostratigraphic

starved required . , as

reservoir grade

work presented in th a shallow

, aquifer appraisal, and CO et al. is in significant , 2014). et al. Longhitano s ) et al.

, and fluvially end members different parts of thebasin augmented tidal range can can be classified as sediments deposited in hampers interpretation of the

encapsulate Roos , 1992; Dalrymple

succession that , 2014) et al. unavailable and

, 2012; and sedimentary (

Godin, 1993; to trigger

-

et al.

marine to with arelative sea & within the context of tidally influenced, , 2018) offers changes in potential in containing

Schuttelaars, 2011; .

et al.

Pellenard the that are , 2012; Reynaud framework, and sa d by the deposited . starved macro Broad, shallow ndstone bodies . trans or

, 2012; architecture,

marginal aeolian is article abandon

Sztan displays succession of ing of (i) (i) relative relative sea and the result of ition et al. et al.

further most s Reynaud

2 the and ó

- , 1992; from & epeiric , 2014) level

become

a

Upper de

- & tidal -

that an - &

,

This article isprotected rights by All copyright. reserved. the Colorado Plateau overlying Upper Jurassic Curtis and Summerville marine Carmel Formation, thecontinental MiddleThe Jurassic 2009 northerly oriented retroarc foreland at basin the foot of the Elko Highlands lithostratigraphic al (Upper Oligocene) also impacted on the Murray Plateau uplift and its sub remobilisation of the 2003). the development of basement Wyoming featuring thin stacked tectonic contraction and extension Nevada border, (ii) the Elko Orogeny (Middle Jurassic), characterised by alternating episodes of Jurassic(Middle 2011; Anderson, 2015; Yonkee Me Four major tectonic events Tectonic GEOLOGICAL SETTING contemporaneous systems in order to fully assess the basin’s history. marine and obliterated by those of autogenic aims: vicinity ofthe San Rafael areaSwell between the Entrada Sandstone, the Curtis Through surfaces for correlating highly heterolithic, tidally influenced sedimentary packages. stage autocyclic processes, within stratigraphic wellas

Accepted 1991;., Nelson, 1997). Article sozoic ) .

i . Consequently, the study illustrates the value in identifying key sequence stratigraphic )

part of The The systems t et al foreland basin

o an setting , and the rise of theNorth American Cordillera (Hintze -

basinal , and (iv) the Laramide located demonstrat s assessment of the sedimentology, and ., 2016). tratigraphy of central surfaces are

the su and thick , -

in settings where Lower Cretaceous), whose granitic intrusions can be observed at today’s Utah

reconfiguration sub Sundance Sea flooded timesseveral during its history c ccession is

The igneous oastal toshallow (Fig. 2 most Paradox Basinevaporitic strata (T - e divisions

development

- that skinned The Upper Callovian to Lower Oxford - regional to regional extensional episodes (Levander probably notably when the tide

have ; dominant allocyclic signatures Gilluly Gilluly - rooted monoclines, such as the San Rafael Swell (Bump

& overprinted periodically by

were , impacted impacted on Utah’s geological

east

Orogeny (Upper Cretaceous to Pal Weil, 2015; and references therein): (i) the intrusive - during the Oxfordian overprint occurs , accompanied eastern Utah was also

a & of south ,

(iii) the Sevier Orogeny (Lower Cretaceous to Pal consequence of allocyclic forcing, but - deposited within the processe Reeside, 1928; Pipiringos - directed fold marine Temple Cap Formation, the shallow to marginal sedimentary stratain central Stratigraphy Entrada Sandstone complexes ofthe Abajo, Henry, and La Sal Formation - central Utah s, ands, - formations comprise by the development of dominated embayment enters a resonant correlation of - , thrust belt

through ii ) and the Summerville

Age. to understand and interpret r urgill, 2011), as well byas the Colorado affected (Fig. 2)

Utah the sedimentary response to in the sediments can be

Identified

a

ia of s

knowledge structures development - n Entrada & & Idaho Trough, aSSW the stratigraphic relationships ,

(Thorman, 2011)

by diapirism and outh

this study the has following O'Sullivan, 1978; Peterson Kowallis, 2009; Thorman, a eogene),

- eastern (Sullivan Utah

- and the San Rafael Group eastern Utah

( SSW Hintze

in Idaho - of neighbouring and Curtis t evidence for F raceable

since the early o - Nevadan Orogeny N associated et al. rmation NE & - Summerville

- - Kowallis, Utah , 2011; , which the

striking, overprinted

,

shallow and Mountains - NNE &

a in the - eogene),

this

Davis, with the -

- of et &

-

- This article isprotected rights by All copyright. reserved. t configu can be et al. accommodation dipping, shallow, and fluvially Currie, 2008; Ogg tidally influenced heterolithic strata (Fig.Swell 2) by Gilluly and Reeside (1928) EntradaThe Sandstone is overlain by the hydroplastic sagging (Zuchuat irregular tidal ravinement surfaces, circular collapse structures, sediment flat angular unconformities wa wavelength varying The Unconformity (Zuchuat t Crabaugh regional base 2009, 2010). that originated sediments sediments ofthe Curtis Formation directly overlie the Slick Rock Member 2015). Kocurek and northwards, toward the therein with 1952) and typically date of160.8 upp 1994; Hintze rusty Formation and warm arid conditions prevailed As Brenner consequence ofdeposition within regressive Doelling Pipiringos, 1979; Anderson he Entradahe Sandstone is capped at top byits the he he s

Accepted Articlethe Curtis Formation ermost (ii) the(ii) unconformity generated by both erosion , 2018) marginal - red to light ,

Jurassic attributed T characterised ) ration, which . he he

& et al. & in The Entrada Sandstone thickens westwards, in the direction of the Utah &

are the main constituents of theEntrada Sandstone Peterson, 1994; Peterson, 1994; Bjerrum (TR) Havho to (Fig e strata strata of theEntrada Sandstone in southern Utah provide a overlying

. The underrepresentation of wave Kocurek, 1998 arth

. Four - & , 2013 ± (i) (i) the Slick Rock Member - The The Curtis sediments comprise level oscillations, are recognised within this coastal aeolian system (Carr marine

. shallow 0.4 Ma from basement rocks of today’s

Kowallis, 2009) sequences 2C) development y - lm, 1993; to the orange,

et al.

f displays ‘ construction acies thins out to ). were from

facilitated dissipation of by ha and partially These

sabkha (Dosset, 2014). , 2016; Zuchuat and ve protected nature of the et al. repeated the overlain aeolian Entrada Sandstone

a

; with , relief Carr epeiric

& Kocurek successions green to white paraconformit , Uinta Mountains

decimetre

- 2018

Lucas, 1994;Lucas, from exposures diminished at starved, epicontinental basin like et al. - . R

related and deformational processes - - an destruction Crabaugh with an ,

ecent

the yet conformab deposits contemporary , eastward Sundance Sea

, , in press

in press (Kreisa the south and ofeast thestudy area s &

extraneously ediments of t Utah In east

et al. Lancaster, 1999; Kocurek, 2003

40 that comprises aeoli to represent amplitude ranging 0.1 from mto23 and m, a Ar/ lower the - & i

Doelling, 2001; colour Idaho Trough es , 2018) ( ), first defined by Pipiringos and O’Sullivan (1978) ’ &

) Witkind, 1988; Doelling end

and southward Kocurek, 1998; Mountney, 2012; Doelling 39 - sequences ( .

ly by , complexly wave central Utah, t

(Fig. 2

along the - hectometre Moiola, 1986; Ca Ar steep incisions,tidal sinuous undulations,

related structures within the Curtis Formation Appalachian Mountains Curtis Oxfordian Curtis Formation,

of the Callovian

regional, polygenetic, and heterochronous J regressed age determinations of informal ation, which

those of five

he shallowhe to marginal deposited as the Curtis vegetated energy ; &

(Fig. 2 Witkind, 1988; Crabaugh

sea Dorsey, 1995;Dorsey, Thormann, 2011) upward - northeast arranged, sensu

, as well as the elongate (Fig. 2B; Anderson

scale

Sprinkel unit unit of the (Yoshida

the marginal C northward that developed he Entradahe Sandstone is divided - an dune and interd ; wedging geometry ,

Gilluly , mottled loess strata, interbedded

is due to the presence of - M indicative of a drainage system puto

thi (Zuchuat ountney, 2006), related to Age margin of theSan Rafael nning

shallow et al. , & et al.

et al. & (Thorman, 2011; Zuchuat and surface types include ’

earthy facies Pryor, 1991; Wilcox

n ; Mountney, 2012) Reeside, 1928; Peterson, during the Callovian Age (Dickinson

tephra layers within - ,

Oxfordian depositional , 2011

marine to continental (Fig 2B) transgressive , 2007). . et al. , 2015; and references ary loading, and - R marine Carmel sea - as the marine ecycled originally & ,

flooded a gently a

& Lucas, 1994; une sediments, in press ; 2011b that

, -

Kocurek, 1993; Sediments of

basin basin Idaho Trough, rate of where & ’ packages of

fluvial (Imlay, is a is

Gehrels - - defined . et al. )

; .

the Relief ,

and & ,

- , the

3

.

,

This article isprotected rights by All copyright. reserved.  1978; McMullen Jurassic system ofthe The Curtis 2018,). Summerville Formation (Fig. 2 In the plain environment andeast to Peterson, 1994; Lucas, 2014). deposits of In the study area(Fig. Curtis Formation ( and contemporaneous equivalent (Zuchuat intertidal deposits, which grade into the supratidal deposits ofthe Summerville Formation upper Curtis conformably overlies the middle Curtis, and channels, sub regional Major Transgressive Surface to the underlying hetero middle Curtis is characterised by a which gravel deposits, grading into thinly bedded, Zuchuat informal units 2015; see (Gilluly maximum thickness of a result, t Wyoming Formation in Wyoming (Imlay, 1947, 1980) 1980; Wilcox For neighbouring areas: relationships between 1994; Dickinson I Entrada Sandstone (Gilluly glauconite and chlorite

t is possiblet is to infer the Curtis sea basin reached approximately 800 km in length (Peterson, Numbers in parenthesis following the names of places refer to localityAccepted numbers on Fig. 2. Article mation A ‘ Four Corner

) & , theTodilto Member ofthe et al. he Curtishe Formation is characterised by an east and south

et al. - Reeside, 192 f - Idaho border (Mansfield , ig. 2 and f S the south the Summerville Formation (Gilluly whereas urther north in ummerville interval corresponds to Peterson’s (1994) fifth

- Formation , 2018). The lower Curtis tidal rich &

, 2018). based

Currie, 2008) et al. & ,

to intertidal dune and flat deposits (Zuchuat Caputo subtidal channels and dunes occur Gehrels, 2003), and at least 150 km inwidth s (Zuchuat f

’ ig. 3 in Zuchuat t the Beclabito Member

, the Summerville Formation up area he he , 2014)

Sundance Sea and the 2), t T 8; Caputo the . approximately

on owards the Utah

The colour Curtis (Fig. 2 lithic lower Curtis (Zuchuat , & he Upper he Curtis overlainis where studied their outcroptheir character:

& the

Pryor, 1991; Peterson, 1994; Doelling, 2001; , and likely corresponds to theLZA et al.

. Itcorresponds to Reeside, 1928; Caputo However, - C

Summerville interval Uinta MountainsUinta area (Fig. 2 ; &

Condon , 2018). the states of Utah, Colorado, Arizona and New Mexico meet s

Curtis Pryor, 1991; Peterson, 1994; Thorman, 2011; Anderson, lighter to strongly contrasts & et al. Wanakah Formation

dark

Roundy, 1916; Pipiringos the

(MTS) 80 at m Sven’s Gul comprises

in - -

, 2018) Color & aeolian deposits that form Summerville interval - coloured and green to grey, heterolithic subtidal flatdepos

what were

of theWanakah Formation Huffman, 1988, ; , and consists of

Western Interior Basin and ado border &

the Redwater Shale Member of theSundance . The Curtis Formation to

laterally restricted upper shoreface to beach Reeside, 1928; Caputo likely formed a as contemporaneous coastal

the lower, middle, and upper Curtis the Stump Formation in th

& et al. is

(Zuchuat conformably unflooded neighbouring regions

with the underlying rus Pryor, 1991; Peterson, 1994). the lateral equivalent ofthe Stump better ch

, 20 is the lateral equivalent ofthe Curtis comprises

(

Fig. 2 ( Kocurek A

9 complex 18). Its base corresponds ; Pipiringos 

), in the San Rafael Swell area sorted sandstone , and equivalent succession in et al. , et al. - & 2.3 third based on stratigraphic )

, these deposits Imlay, 1979; 1980)Imlay, - by

wedging geometry , 2018) , 2018). The dark green, (Pipiringos the thinly bedded, sub et al. arrangements dark brown, sabkha

corresponds to the is (TR) Moab & -

& , 2018; separated in Zuchuat order

Pryor, 1991; . The overlying Imlay, 1979; Imlay, cycle withincycle the ty Member oftheMember e vicinity of the - TR & red by Zuchuat form

O’Sullivan, et al. - interval of comparison

of subtidal

terrestrial to

, to lateral to the

, 2018). tidal ( with its in

Fig. 2 three et al. the

. As to a

;

,

This article isprotected rights by All copyright. reserved. sequence stratigraphic ravinement surfaces ( transgressive surfaces, regressive surfaces of marine erosion, flooding surface means of Merging sedimentary data withphotogrammetric models and structural data sets and Aberdeen Limewith PhotoScan Pro photogrammetric material (after Westoby interval of interest, 3D virtual outcrop models were produced from the collected order to the visited localities This sediments dominated successions (Fertl (Th/U) these data must be considered within involvement of extraction g section covering the Entrada permit interpretation of depositional settings. lithofacies analysis and architectural fractures and faults structural information w pal logged across the Entrada were area Swell, Hanksville, and from Last Chance Desert 5) and dataThe necessary for DATA (2016) t Haq amma

Accepted Article, north ofthe San Rafael Swell, a eocurrent 2018 et al dataset systematically visited eastward - ratios as a discriminator of marine over continental provenance arereliable i AND ray spectrometer in fullassay mode at 20 cm intervals ime document, illustrate . (1987), post calibration . tracing ©

The The areastudy as well (Svendsen , asoftware developed by

or the marine influence marine the or t scale is and horium (Fig. 2) METHODS

u © readings complemented by niversities

to Big Pinto Mesa (Agisoft L . key sequence

, as well as along the

. using Of these, 41 sensu

this study framework and u were as ranium values, which which values, ranium

in central - LC, St.Petersburg, Russia)

standard, handheld cameras, Curtis

(Bonaventura

collected, Catuneanu, 2006; Catuneanu -

& and understand the Curtis collected exposure of the et al.,

the

stratigraphic surfaces Hartley, 2001). -

southward

s outcrop aerial images,aerial Summerville stratigraphic interval were gathered during three field campaigns between 2015

onto Wilcox and Currie’s (2008) age and Og ( magnitude over the over 30 - - 1982), yet they remain relevant for coarser eastern (Fig.Utah 2) extends from Summerville interval were logged using a hand - the Virtual Outcrop Geology element analysis (Walker, 1992) including the

) the context of the sediment calibre:

from on interpretation (38 et al.

sections were

the Utah paralic et al.

to Notom Ranch 3D

and were

Entrada of

, 2017; Buckley To augmentTo the sedimentary detail, 35 of m

, 2012). The models were generated using photographic material collected at and between exposed fault

39) deposits ( deposits

complex 3D sedimentary architecture ofthe used to to used - dip dip and dip Colorado border. , before being analysed and interpreted

, such as subaerial unconformities, displacement on the western margin of theSan Rafael - .

Curtis

and measured dunes and ripples determine determine et al Fertl

unmanned aerial vehicles ( -

(35) Summerville ., 2009) et al. .

direction The g et al., , 44km ( and s , 2017) VOG the . . amma

Standard techniques in In order to cover the study

A total of 1982 to provide a

degree of degree were used in order to a total of2291 werem the )

group of of sedimentary strata, southwest . t -

. interval ). d ray h Humbug Flats

A orium

I dditional nterpretation of g and others’ s, s, 869 -

ata allowed for the the for allowed ata continental grained and both Bergen / regional provide ,

u 43 - of held tidal ranium n mud

lo UAV calities

(1

d -

) a

to

. In

This article isprotected rights by All copyright. reserved. sandstones are ( modified as Interstate 70 Description Association2 Facies provenance (Fer suggest a more prominent marine origin for these sediments developmentfluvial is lacking withinthe Entrada Sandstone. depositsflood and some episodic fluv Curtis sea, and the accompanied deposits settled as the flows decelerated. Except for these flash of theunit aeolian dunes migrated and loess were like environment whereas the contemporaneous FA 1b Interpretation well are infil Unconformity of FA ( eastwards in the vicinity of Moab (Fig. 2) thickens stratified sandstone fine facies of theEntrada Sandstone, and Rock Member consists of associations that are broadly compar Description Association1 Facies relationships. history ofthe basin development ( Forma work faciesThe RESULTS Fig. AcceptedFA 2 Article 1 - -

grained 5 rounded extra is ; su ) Fig tion and its neighbouring units capped by provide led with mmarise north s

(Table 1) and facies

are interpreted the as product of flash floods predating the tra mostly 3 : :

a

The Entrada Sandstone In the northern and western part C and sandstone

n (12)

: of theEntrada Sandstone. described -

approximately FA 1 westwards

plane parallel t matrix tl horium/

Pipiringos and O’Sullivan

Zuchuat at the fringe ofthe Slick Rock Member palaeo

the polygenetic

cross and Shadscale Mesa et al.,

4 - , a

, basinal and to ,

evaporitic beds – – corresponds to acoastal wet aeolian Table 2)

- , with BeachUpper to Shoreface Deposits Coastal Wet - supported, chaotically arranged 1982). stratified by u et al. , and pinches out southwards around Notom Ranch

ranium identif pebbles and cobbles Zuchuat Zuchuat inter - ,

stratified 2 mt locally deforming its substratum by loading. ’s associations (FA) scheme

(2018 , heterochronous, and y digitating aeolian dunes and interdune ratios of

h depositional environments

at the bas , and isolated dunes Ae et al. ick, ick, comprises able to . ial terminalial splays (Valenza, 2016), evidence for major strata were deposited within

Combined with an understanding ofthe J (13) ) detailed sedimentological assessment of theCurtis olianDeposits

intermittently and

laterally restricted FA 1b . , in press),

P

(1978).

rocessed , t approximately 5.

planar to trough cross the unit’s he s e ofthe studied interval

c of the study area

parallel surface orresponds to therusty

(Fig. Locally, Locally,

t g hey 6

low amma deposited lithostratigraphic A, B and C -

diachronous (Zuchuat

of laminated to mottled

s conglomerate ( - are

- stratified sandstone, rippled cross Fig (Table 2)

angle cross the J dune

erosive scours at the top of the

(200 -

s , ratherthan a fully continental ray data from Duma Point (19 use The

3 -

- and their deposits belonging to

A, B and 3 Unconformity erg , notably at Sven’s Gulch system (after Mountney, 20 . d to decipher the dynamic - ) The 500 m) t .

horium/

, where isolated coastal a which

marginal - erosive scours

s stratified comprises , -

comprising

subdivisions red, informal earthy spatiotemporal

4 nsgression of the fine , are developed u Table 2 T ranium ratios he lowermost - silt

grained sandstone - (35) et al. marine , which - wa 3 Unconformity

stone two ) , and s locallys , .

rounded to

in press FA 1b at the top . the facies , sabkha FA 1a

and very are

(9)

in this Slick Slick FA 1b

of 5

) , 12

- )

J - - ) 3 ,

This article isprotected rights by All copyright. reserved. absence in the deeper and distal more part ofthe basin, denotes occurrence ofRSME’s in the more proximal pa conditions accompanying the development of theabove thefrom basinward migration of subtidal environments 3b of the shallow and are interpreted as parasequences, environment. area (Fig. 2012). Interpretation substrata by a butsharp non drapesmud between foresets (Fig. H sand well base In the north oft et al. Unconformity erosive widem and deep10 m incisions into its regressive surface of marine erosion gradually transition and deeper part of the system in the north (Fig. sometimes thicknesses flaser characterised by proximal and southern part of theshallow northern, distalmore part ofthe system a varying sand and are Description Association3 Facies shoreface deposits represent the oldest deposits of theCurtis Formation (Zuchuat Interpretation loading structures ( overlies FA 1, from which it is separa and rip overlain by trough cross eterolithic gravelly dunes arranged in thin

Accepted, Article

correspond to regressive surfaces of marine erosion (RSME; Fig. - s , , rounded, gravel

- in press with and flat upper bedded

The The - character up clasts are documented at Interstate 70 dominated by thinly bedded and laterally . 4

green mud

) : erosive three

of 3 Sediments of indicate

) , as they don’t erode into the - Each ofthe three upward shallowing packages are bounded by flooding surfaces, : : siltstone and . -

marine system, the erosive surfaces

FA 2 represents FA 3 to he studyhe area, -

10 cm abundant upward - , mud ratiomud deposits of - surface erosive flatbase, and co Fig. 5

heterolithic deposits testif and coarsen

surface - an increasing energy level within a gradually shallowing subtidal flat – size, extra drapes

. The base of FA 3a Subtidal - ). stratified sandstone and/or - FA coarsening trend

. The base of ,

bi sandstone , ranging from mud s

3

locally (Fig. - FA 3a and FA 3b cross

directional overlay FA tidally - Heterolithic Flat Heterolithic basinal clasts

upward from 6 6 - A and D stratified, A and E

observed ted by the J in the proximal part of the areastudy -

strata influenced upper shoreface sensu FA 3beither is conformable , substrata

to sand

ripple can can be 2 (or the J - underlying strataofthe marine basin s ncave down top surface, migrating on FA 3 ) -

)

observed

Catuneau thick

(Fig. form part of FA3 are also present

rt of the system, contrasting w within a offinematrix to very coarse between th heterolithic y are often preserved FA 3a to FA3b. -

4

dominated ( - of osc - cross

grad 3 unconformity, which can locally display ) dominated - extensive 7 ( (12) where up to three stacked thin cyclical bundles, with c , Fig. 3

A, B and C sometimes observed at the base - 3 unconformity where FA not 2 present)is ripple ational - illating energy notably laminated et al. and Uneva Mine Canyon

mentioned parase E characteri ( Fig e gravelly foresets ) , .

bedforms -

, heterolithic subtidal D (2009). laminated sandstone FA 3a , or ( s espite their intraformational ) FA 3b

. These

. It 3 . in the northern part of thestudy The in A D and

can can it it a ,

bed

cross ) basinward corresponds to

deposits. sed by higher , commonly observed in the passively onlap Entrada ) , as visible in the more distal

In the more proximal part also , prevailing in the more 4 , with concave up, erosive

within the system deposits fills

typically ). These RSMEs result 4 - ; stratified

Table 2 correspond

comprise , capable of quences

Sandstone

These upperThese (Fig.

ith theirith notable - succession increasing slope

are characterised entimetre reach

) (14)

. FA energy , . Muddrapes deposits

7 a sharp lenticular ping e

. The D rounded to - t al.

grained . FA 2 es of the FA ) to a 3 is .

cutting

(Zuchuat

, 20 the J ( s -

Kvale, thick an , 18). with with

- to d 3 45

This article isprotected rights by All copyright. reserved. ( T in the northern part of the study area, to Zuchuat New can be which Description F 4 7 tidalsteep incisions (Fig. 3E). Despite evidence of current reversals within the sediments (Fig. Sven’s Gulch (9), Cedar Mountain (43), lower Curtis, constituted by FA 2, FA 3, and lowermost FA 4. The parasequence, occurs only at interpreted contemporaneous and neighbouring colour ofFA 4a are thewithin uppermost parasequence correlative, more distal, gravel Interpretation flow foresets rounded, gravel size extra 10 m Fa unidirectional current ripples and herringbone cross plane parallel characterised by a Rafael Swell fine Description Infill Association4 Facies tobasin the south unseparated and relatively 3a basinward part o are interpreted as subtidal channels. Their gradient. Fig. acies Association5 acies B A and C he

). 4b is restricted4b is to the north

Accepted Article(Fig. se -

grained ripples climbing on the reactivation surfaces, 7 Mexico thick, multi

E through sediments comprise represent erosive 4 ,

et al. ), the lower Curtis is dominated by a basinward (northward) current direction (Fig.

reactivation surfaces, as well as bidirectional current indicators ) The bedforms, concavewith up, erosive bases a ,

highlights the separation of thefl : :

to reflect the most prominent basinward shoreline progradation recorded by the , in the , where it marks thebase ofthe Todilto Member of the Wanakah Formation FA 4 The lower Curtis is sandstones , 2018; - : FA 4a and FA 4b represent a proximal sub . laminate

It s thes I

- f the system, interbedded between mud can is ) stor , . Grain size fines southward thickening which otherwise lead

southern and potentially related to thereworking subdivided

Zuchuat

– – be informal middle Curtis e

y Sub Sand d strata, with single ,

tra

that extend coarse -

basinal clasts (Fig 3

tidal light green to white, very fine to fine ced throughoutced the study area higher higher energy condition - Rich et al. - - eastern margin ofthe San Rafael Swell in rich, subtidal channels, respectively (Tabl

- overlain to Intert to grained more proximalmore to Subtidalto , in press slightly

FA 4a

over tens of of thelower Curtis (Parasequence 3) aeolian dune fields

and Sid and Charley (41) (Fig. 3D).It is characterised by ,

disconformably idalChannel to the deposition of better sorted sedi approximately cross (from

and

) restricted south and eastwards, where FA 5 dominated is by and double . ow in the system. This is in contrast to

The unit

Supratidaland Flat CorrelativeTidal Channel FA 4b - G stratified sandstone 4 to 15 ). It displays common part of thestudy area (Fig kilometres on the eastern margin ofthe San

t (

hickness of Zuchuat and herringbone cross s observeds . FA 4a -

occurrence in the more distal and - stratification. Dune

m mud drapes,mud

of

1 m, as1 m, itthins south and eastwards o - by nd flat upper surfaces (Fig. tidal , alltheway to Ghost northernRanch, f the thick dominated heterolithic deposits ofFA

fringing

et al. comprises - FA 5 FlatComplex Description

FA 5 varies from more than to supratidal sandflat, and the

S ) in the more proximal part -

lick Rock Member , 2018). Its base of plane parallel grained

(Fig deposits of

with rounded to well along with rare, s , where it consists of mud drapesmud along

light 3 H and well , such as e 2). FA 4 onlyoccurs - . The grainsize stratification s - pink, very

2 -

sorted

and 4 the ments A

is sharp, and it - , bedded subordinate . Table 2 Table

FA 4 3 the

F 6 sandstone

) (FA 3b)

A and D fine to fine .

.

FA 4a

is

(Fig. 2

and the s to )

4 of the a 5 m . 1 to

) is - ;

This article isprotected rights by All copyright. reserved. FA 5. (Fig. 3 Curtis Interpretation minimum of northwards,thins areastudy ( up stratification. Individual bed set thicknesses range fr by plane stratification,parallel unidirectional current ripple and herringbone cross of Description Association Facies marine system surfa recognition of any traceable stratigraphic surfaces, such as flooding surface the underlying lower Curtis strata energy level subaqueous dominant arranged in tidal bundles to intertidal channels and associated tangential to sigmoidal cross transgressive surfacebasal corresponds to theMTS Interpretation of current motion at the time ofdeposition, oriented NW 5 Curtis deposits. average bedform size distances of low deposited as single ordouble drapes. mud to metre cross packages sporadically in sandstone very fine to fine

thins tervals dominatedtervals by bidirectional herringbone cross

green, silt Accepted- Article section - angle cross

ces of marine erosion - stratified and wavy to flaser

I (

, Table 2), in these directions Zuchuat -

scale tidal bundles with v are observed within FA 5,frequentwith bidirectional current component s

(Fig. 3 : , with , with occasional laminated mudstone Fig , evidenced

stone The middle Curtis FA 5 deposits are conformably overlain by 5 to 40 m. 3D 5 m within the succession - : : ravinement surface

. s 4 s and FA 5 corresponds to the informal middle Curtis unit (Zuchuat FA 6

- - dunes B et al. stratified grained

at Sulphur Canyon (1) reflect I edform

, Table 2) to fine from a

6

constitutes the informal upper Curtis

– 2018) is

within a sub

8 Individual bedforms in FA 5 reach amaximum height of 2 to 3 m, UpperSub Heterolithic

ing by coarser ; one to two - sandstone Zuchuat . thickness grained, laterally extensive, isopachous sandstone beds, distinguished maximum thickness ofapproximately 28 nearm Hanksville

. intervals. These facies This This indicate

, accentuating the contrast thewith underlying lower Curtis shallow Pal

a . . FA 6 It was depositedIt was lower energy environment with respect to those oftheunderlying a eocurrent measurements indicate a crops crops out et al. . FA 5 is interpreted as . - , arranged in a near orthogonal pattern. - arying amount

tidal

bedded sandstone strata are T . FA 5 features grained and better order decreases he amalgamatedhe bedforms and bedform sets ( , 2018). Zuchuat s

(Fig. to intertidal system.

strong cyclical tidal influence on the system s

of magnitude higher than in the underlying lower FA 5 also comprises p

. in the northern, central, and southern parts of the Subtidal channels erode 4 within sub up )

tidal Unlike .

et al. - laterally s section, as well s

lenticular to wavy to flaser . It comprises also climbing ripples, reactivation sur

of organic

to Intertidal to Flat , 2018) om 3 to 40om cm, and beds become thinner

the - sorted sorted sediments than compared with - tidal stratification. Interference ripple - an intricate SE underlying , conformably overlying the middle inter

, which is a composite surface

(Fig. FA 5 reflects an overall higher

/argillaceous to intertidal flat environment digitate withone another

locally lane parallel as 4 - faces B stratified sandstones

strong bi south and eastwards, as d )

amalgamation sediments of .

in arranged in and to sandflats and FA 6

3D matter, often s

counter -

- or regressive - modal distribution et al.

bedded stratified c ,

ross which inhibits the

, 2018). Its FA5

- - centimetre

of sub - stratified

ripples with

(34) and consists , FA 6 , and

and over s

tidal a

s to a occur . The

FA the

-

This article isprotected rights by All copyright. reserved. starved aspect of t t that punctuated overall regression light grey, marine Curtis Formation supratidal, paralic to Interpretation m fall the beds. thicknessThe and the frequency of these deposits diminish up FA contains 8 also c underlying strata of deposits Description Facies testified by the development ofrhizoliths in the underlying These supratidal deposits are often associated with of local sand stromatolite structu towards the eastern and more continental part ofthe study area,linked with the development found overlying these supersurfaces, whereas supratidal deposits become more frequent aeolian sequences. Towards Duma Point (19), su supersurfaces (sensu Kocurek, 1988), implying that of theCurtis Formation (Fig Interpretation crust on top of these erosive surfaces packages cross 2018). traceable Spring Canyon stratified sediment deformation structures stratified characterised border, and pinches out between Duma Point 2 Table Description Association7 Facies horium/

Acceptedin width, Article at approximately 5. t horium/

- that is stratified

Association8 These These ) .

that . FA 7 reaches a maximum thickness of u

dunes sandstone erosive surface U ranium values of approximately 5, similar to : :

ndulating m and 0.5

Towards the parteastern of the study FA 8 typically

u sharply erosive surfaces , : : FA of 7 consists aeolian dunes corresponding to

ranium ratios

at baseits (28) FA 8

sandstones , reaching a

. These consists of - he studied basin is further emphasised by the scarcity influenced str -

entimetre 1 m s on the eastern border ofArches National Park. belongs to theSummerville Formation FA 6

, interbedded sabkha – – structureless overl

CoastalEolian FieldDuneDry Supratida O illimetre

in depth were likely , , under which abundant rhizoliths can b nly

sub by very fine to fine y n with s

-

the aeolian dunes of rusty red to dark brown, evaporite pro three

individual tidal like 3

to d can can be J and .

cessed from the g

ata testifies

The . single and double to c

l Flatl res similar to those described by Getty and Hagadorn (2009). . FA 7 sediments

ecimetre to supratidal sediments

. minor channels were observed within FA 8, reaching . The marine influence ofFA 8 is with

8, 2). Table The traceable erosive truncations are deposited

en uppermost overlain

timetre is composed offive maximum green silty sandstone - thick, light grey, ripplecross that - to the grained,

(19) by - as the scale, approximately

package

b overly very fine to fine FA 7 amma tidal

thickness of area frequent and recurrent marine incursions and Horse Flies Gulch mud drapesmud

sparsely the

Curtis structureless

. structureless to ripple to trough cross

T to intertidal deposits are commonly ,

values

the shallow - Moab Member consists offive stacked FA 6 is replaced by he ray data collected at Point Duma (19) is also overlain by a sandstonethin is grad is , and mainly consists offine

packages contact between strata. sea regressed.sea The occurrence of

vegetated palaeosol horizons, as s

, commonly displ observed in FA 1b 50 close tom the Utah , and approximately - Doelling’s (2001) Moab Member rich e - ational grained, ripple or

observed

sandstone strata E supported by -

marine deposits arranged in flaser -

ach mudstones and siltstone of section. section. fine

- package

(Fig. 3 and the limited size stratified sandstone (20) - FA 7

grained,

FA 8 and the (Zuchuat Similarly to FA 1b, . 15 It is It is I and K aying soft , -

.

(

is 20 at m Lost The fluviallyThe Fig

capped by

herringbone also occur

cross of the - s Colorado et al. -

- Table 2 3 bedded grained

J and 30 -

- 50 - of

8 ) a . ,

This article isprotected rights by All copyright. reserved. (2014), as the deposition of the Entrada Sandstone, the Curtis, and Summerville formations, and (Zuchuat J The Pre shoreline influence low history ofthe interval is more intricate than that previously proposed (Fig. stratigraphically diverse body ofdata assembled here suggests that the detailed strat This supportsstudy their interpretation as a general conclusion, but the spati transgress Several authors have presented the Curtis and DEPOSITIONAL MODEL time highly geometries geometry can be produced by different processes, and one single process can generate different each in a 3D space regressed ravinement during transgressive phases, and funnelling ofthe ti processes Interpretation the MTS at the base of the middle Curt (Zuchuat200 m a from c ( including fault unconformity, deformation Formation Description J neighbouring shallow the - g 3 Unconformity3 Accepted Article) sedimentary loading, and ( - - fluvial channels Curtis gradient systems like the Curtis basin the

- barrier, and thus, as an unconformity individual process and indiv 3 Unconformity is intrinsically polygenetic, heterochronous, and diachron polychronous nature ofsuch asurface implies entimetre d et al. . It is important to notice thatt , which includes aeolian deflation, superficial incision linked to flash floods, tidal and ive

sea by the effects of is characterised by eight different types of relief related to (i) : The J

( - Burgess , but they varied with time related - , :

regressive (Caputocycle -

by consequence ( 2018; transgression The J The plane and erosion b) paraconformity, (c) incisions,steep (d) undulating relief, (e et al. -

- 3 Unconformit scale, to amaximum amplitude of whereas 23 m, observed in outcrop -

processes 3 Unconformity composite surface, is in press , in press). & - marine

Prince, 2015 relatively relatively minor changes in sea

), comparable to the compound surface discussed by Ahokas h domain , .

) hydroplastic sagging the facies distribution The To theeast of the study thearea, J y, which separate - idual type of relief arenon related relief irregularities, ( ; Zuchuat different types of relief . is.

& , both in terms of intensity and location

hese different processes did not within this paralic system, contemporaneous to the

Pryor sensu stricto et al.

interpretation of stratigraphic detail is Summerville formations an as overall ,

1991 s , in press

the Entrada Sandstone from the

that ;

( (Zuchuat (Zuchuat Wilcox . Midtkandal

it it cannot be reg

- the product of

level ) are - . Therefore, the composite and unique, a as & f

) cir classified as (a)

et al. dal forces as the Curie 2008 upon the position of the - 3 Unconformity merges with & cular collapsed structures, its ,

Nystuen in press). relief The ranges

wavelength

erosive only impact the system

specific arded a genuineas series of 9 ;

Peterson ). ally and , ) irregular relief,

I 2009) . Further mportant angular ous by nature , or (ii)

shoreline relief

erosive can can reach Curtis .

igraphic

, strong

1994). more ly et al.

, in ly ,

This article isprotected rights by All copyright. reserved. sand area FA 3a mud remains unconstrained. Curtis episodes parteastern of the study area remained unaffected by the ma the system diminished proximal domain ofthe study area t The in press however sedimentary explanation for Nevertheless, a subsequent transgression (Fig. highs within the Entrada Sandstone acted as interfluves (14) constrained to certain localities (Curtis Point earthy facies The oldest sediments of the Curtis Formation developed during the earliest flooding ofthe Early al. accompanied by the development of theJ aeolian system in t influenced by marine flooding the as early Curtis sea linesThese of evidence together support an interpretation of theearthy facies partly as strata recorded values in this study of approximately 5 indicate marine influences over these paralic < f Unconformity An the as Curtis sea started to transgress from the north. suggested by Mitchum surface. Consequently, the J the accompanying relative sea facies offacies theEntrada Sandstone, but also in acies acies of theEntrada Sandstone at Duma Point 7 , in press), rather than an unconformity

Accepted Article can can be used to indicate interpretation of ) , -

ransgression continued, and reached areas , it represent dominated Curtis .

(Zuchuat U

) can be regarded as evidence for pre excess , , which generated low

be linked to pre coupled witht - do sea

, and correspond to FA 2 shoreface deposits. calculations minated deposits is s FAs 2 a tidally influenced et al. t further FA 3b ransgression he southhe and eastern part of the study area(Fig. a composite, polygenetic, heterochronous, and diachronous , 2018 typically

et al. and strata are strata

he erosive nature of the MTS that accompanied deposition of the middle supported by preliminary

- clearly clearly transgression, sub marine influence

, the -

’s (1977) definition of unconformities, but was primarily developed in press 3 Unconformity not is the product of a

the -

- overlies level variations, allinfluenced the genesis ofthis bounding subtidal 9 , which amplitude and long wavelength relief

B existence identify cycli concentrated ) . The . The exact natur (Fig distal domain ) , mean that the weste

s 2 s and 9C are more common in the northern parts ofthe study

deposits ofthe heterolithic successions - 3 Unconformity as a ravinement (Zuchuatsurface

sensu stricto of

s withins sedimentary rocks the supratidal deposits ofthe Summerville deposits. - -

existing

regional folding and tilting episodes pal (7) cal

(19) towards a , Sven’s Gulch around marine flooding

) eo of theCurtis sea . transgressionAs progressed g

e ofthese pal ( - amma topography Fig migrated southwards and into a coastal relief on relief the

. earthy facies (FA 1b), a pure

s

the more proximal that Hanksville

5 As - rn extent of the transgression

ray d and

t remained unflooded until the rine flooding. hese sedimentary are bodies

(9)

8 ata obtained the from

of FA 3 ). seems a

(Fig. , whereas J , and eo - As As

, forced regression, as 9 3 Unconformity, as pal which represent - A and B . highs remain

t horium/ 5

Uneva Mine Canyon ( unli ) were deposited Fertl

in the earthy

Sub domain kely the ) . wasThis et al., - u coarser regional uplift . They ,

ranium ratios

J the energy of

- ( 3 s Zuchuat

ly 1982

of tidal equivocal s

the most

e could

arthy . grained

) T , a he eo

et al.

et - .

of , ,

This article isprotected rights by All copyright. reserved. between Interstate 70 arrangement of paraconformities and disconformities (Zuchuat present day New Mexico border (Zuchuat level rise which completely flooded the study area (Fig. topThe of thelower Curtis is capped by the MTS as a consequence ofan abrupt relative sea MajorTransgression proximalmore counterparts were times, some ofthe distal parts ofthe basin However, despite increases in the amplitudes of relative sea of channels sub of therelative sea development ofthe consequence of The steep incisions Consequently, thethree upward flooded the as relative sea proximalmore the north (Fig. sur proximal and shallowest strata the facies belt across regressive surfaces of marine erosion shallowing succession variations major upward foresets, suggest a strong basin Pal tidally influenced environments, in which higher energy tidalcurrents localities north ofDry Mesa exclusiveThe occurrence of thegravel Dalr observed within modern proximity to the coastlin theseas Mountain 3a). characterised by better influence

Acceptedthe most pronounced Article a faces of marine erosion are absent from the most and distal basinward part of thesystem in tidal eo ymple et 1992;al., However, occasional less - current in , which

to supratidal sandflat

(Fig. 3G) in the south influenced by relative sea

(43 in relative relative sea ), - 4

shallowing

part

sometimes show an show increase in the degree of sorting and grain size with increasing a ) ; a consequence dicators the from lower Curtis (Fig. short -

level va prograded basinwards

s (Fig. 3E) de second parasequence

of the basin.

the

s (Fig.

(12) - Harris

- in the more proximal part of the system (Fig. lived sorted facies belt shift

e are in direct contrast to theclassical ‘coarse to fine - -

low level localities within t day, tide

- riations increase up successions level rose, and are thus bound can can display a succession dominated by FA 3b. Textural trends , Shadscale Mesa 4 (6) ; , as FA 4b subtidal channels , decametre scale fall in - gradient Zuchuat et al.

deposits (Fig and coa veloped at the top - of and Last Chance Desert floor ebb - shallowing successions represent of higher

These These upward each upward - s , 2002; dominated environments (Fig. 1; Boyd et al., 1992; -

4 level variations during the development of

. and et al. - Curtis Each of rse that characterise

ri

(Fig. 3F) recorded thewithin lower Curtis (Fig ch dunesch and conglomeratic -

during current overcurrent the area r (P2) Fan, 2012). et al. 10 directly adjacent he morehe distal domain of theCurtis, such as Cedar slope

, 2018). grained deposits compared to the distal setting

(13)

). sea - these surf

section T , 2018; (Zuchuat - shallowing succession , and correlative FA 4b gravel - raceable

, gradient basin shallowing successions the uppermost parasequence (P3 and of The proximalThe

the lower relative relative sea 4

Uneva Mine Canyon

in press , (Fig. 10) )

followed by the deposition of the most

(38, 39) 9 and aces the lower Curtis et al. did did not ed E erosive surfaces within s

), and the area as far south the as in the distal

by flooding/ravinement surfaces. to Cedar - basinward orientation of dune

level variations during Curtis testif , 2018; most ). This

such that

(Fig. 4 - et al. (Fig reach these distal areas level sediments (FA3b) y para parasequence (P1)

to .

in press , 2018; surface a complex is Mountain 4 6 subtidal

B .

that accompanied ) ), may be symptomatic of major basinward shifts of

were in operation T areas compared with ) sequences ( are interpreted as . hese regressive

were subsequently

reflect FA4 Each oft

(14) in press ). - a - s

grained’, trend

channels at the rich, subtidal amplitudesThe

, as well, as as Cedar proximal, 4 (43) P3 s ,

short the 9D he

) than their

, as a , as result P are

). The area (

and 1, upward three Fig. 1 -

are lived P .

2, P the . 10 such 1

a (FA - ). ) 3) - . This article isprotected rights by All copyright. reserved. infill dune field. The of theaeolian system, and transgressive phases partially inundated and 19 T palaeosol and (Fig sequences a As coastline progradation, accompanied by increased sediment availability for aeolian transport. and asymmetrical, eastward bedforms protected zones ofthe contemporaneous marine system, and FA 5 sediments with metre Fig. Kocurek the concomitant development ofa dry aeolian dune system theAs Curtis Curtis middle Curtis sediments and upward m the Sztan significant interpreted the as onset of resonance tidal within the Curtis dramatic shift bedforms, coupled with A the Rock Member resulted in the 1992; Dalrym 2018), as is common in many modern toward the coastline and the middle Curtis thickens toward the distal basin (Zuchuat thewithin H surfaces, and sandflats with astrong bidirectional current component The sediments of FA 5, particularly subaqueous dunes with truncates lower Curtis strata withan angular relationship. Major Transgression Mounta he

) a di

Accepted8 Article are in stark contrast to the underlying lower Curtis andstrata suggest a higher energy level ximum f

signatures of middle Curtis se 8 stinctive characteristic ofthe s 10

the growth ofthe

result,

of the contemporaneous marine basin ; Mountney 8 ó

five sequences of the Moab Member sea ).

& and in The calm and restricted setting for

& de Boer, 1995; Yoshida

were deposited in the distal setting to the west and north (43) ,

Regression marine ( sedimentary Lancaster, 1999; Kocurek, 2003

suggest suggest that looding FA 7 10 sensu - fining of sea

ple (Fig. 10) ), rhizoliths in sedimentology (Fig. 1 abrupt termination

and , thickens eastwards, and

retreated autocyclic

et al. 2006 Kocurek 1988) ( system Fig s by correlative supratidal deposits, urface (MFS) across localities in the lower Oxfordian 1 FA 5 s

aeolian dune field , 1992; . ), shows evidence of ,

4

2012) - a

response to allocyclic f the towards the pr

pinching FA 5 and FA 6 deposits, overlain by FA 8 and MFS by

deposits, well as the as overall up rapidly

processes dominate the sediments absence of traceable

midd 8; Harris reworking ofthese during is likely to Dickinson within

et al. separated by sub middle Curtis le Curtis times from the easter of et al.

which episodes ofrelative base dune fields of , 2007) - day, tide an elongated, semi esent day Utah s ofFAs 7

, 2002; its fiveits be located within the & ) likely sub by FAand FA 6 8, FA 6 strata , neighboured by an extensive

(Zuchuat Gehrels, 2009 .

Because the system orcing by processes autocyclic - - is the amalgamation of cross regional dominated environments (Fig. 1; Boyd

distinct aeolian packages Fan, 2012).

stratigraphic surfaces aeolian dunes reflect humid ( (Fig

Moab Member n inundated coastal plains, the system saw tidal (Fig FA 7 s et al. -

s 10

Colorado border as well as suggests deposition

to 4 ,

(Fig. early Oxfordian uplift prior to the

and and intertidal deposits in western its parts -

, , 2018; enclosed basin of

2010). (FA7; associated abundant reactivation - sea sea The section progradation of the

suggesting that

9 10) 12) , it , it is impossible to trace - lowermost few metres ofthe H arid arid climat sediments resulting ; partial flooding )

by local development of . However, upward Fig . Kocurek

enters in press contrasts with thegradual Grain sizes generally fine

(Fig s - level fall

8 (Fig

(Fig

s terminated the aeolian and ( tidal resonance, and

Zuchuat

8

in

), e may be interpreted as supratidal flat (FA 8, into s 6Is and

& , supratidal sediments,

s

in the proximal and variations 9

as the MTS

overprinting ofany -

9 this size 4 Havholm, 1993; stratified F and

a major climat G (Godin, 1993;

and pr the ),

of theSlick o suggest et al.

mote

deposits of

7 10) 12 E through -

may may be thinning, et al. ). The . Such (Kocurek , 2018).

et al a d

- growth rapid scale , ., e a

,

This article isprotected rights by All copyright. reserved. terminated by marine flooding in the areas close to the pal visible in the vertica which these sediments supratidal and coastal aeolian systems, allocyclic processes were responsible for therate at In Mountney, 2006) associated climat and FA 8 were strongly influenced and modulated by allocyclic relative sea contemporaneous and resonant tide (FA 7) Formation (FA 8), and accompanied by the development of dominated the marine system (Figs 6, 7 and 10). However, retreat of the Curtis generated by allocyclic relative sea and allowedthe system to enter a tidally resonant flooded locations beyond the extent of the MajorThe Transgression and the resulting MTS, which defines the base ofthe middle Curtis, regionally traceable stratigraphic surfaces. eachwithin ofthe threeparasequences (Fig reorganisation probablywas responsible for local incisions and/or continuous deposi part of aself changes in basin 11). The heterogeneous energy distribution of thetidal system was responsive to minor respond During deposition of thelower Curt autocyclic processes upon sediment dispersal and the preserved strata. present an ideal candidate forfuture work that could and transgressive deposits, into the post continuous the ravinementwith in the sedimentology thewithin studied interval 5, relative sea Summerville interval was Sedimentary and relativeofTheinfluence and autocyclic allocyclic uponprocesses system the deposits system that shift

8 and Acceptedaddition to modu Article associated a final, short as anas explanation for the termination . Contrary to thedominance ofautocyclic process ,

preserved e 10; Zuchuat

to su d

to both auto - sedimentation level variations and climat - sustained feedback loop ( pratidal deposits strata ofthe Summer

- morphology, influencing the sediment dispersion and bedform development as e . Gamma lived marine transgression

it oscillations (Fig lating the

l stacking ofthe in its form,final and et al. diagnostic . The marine influence upon the the accumulated cyclic - , ray log influenced continuously by allocyclic processes, most notably by

coastal aeolian systems in press , with no, with obvious periods ofnon from thefrom earthy facies ofthe Entrada Sandstone, through lower Curtis

and alloc morphology ,

with of the J

data presented here indicate that the Entrada ). The s - is, the system was level variations were not preserved, as autocyclic processes

-

8 -

ville Formation. aeolian sequences of the and the cyclic the localised sand stromatolite structures Major domi

and yclic processes e sensu - 3 Unconformity

changes, but by also sub extensive Gamma deposited

, nated system, autocyclic processes impacting on FA 7 10; present of the dune fields

- scale, Transgressive middle .

Cecil, 2003; de Boer

10), shut down the Kocurek -

ray log and type of bedforms occurring withinthe in

of the supra stage. Traceable study area(Zuchuat arrangement

contrast to regionally significant and a thin interval (<1 m) of shallow Consequently, the succession

sediments ofthe anal ,

n as observed at &

o (Zuchuat

acting up

- data (Fig. Moab t in tidal resonance tidal flats of the Summerville Havholm, 1993; Kocurek, 2003; yse a -

deposition or erosion documented eo

sediment supply to the cannot be justified

Moab Member relative dominance ofallocyclic or -

coastline, Member of the Curtis Formation

of those - et al. - regional uplift episodes ( on the deposits ofthe et al.

8 and up stratigraphic ) display cyclical patt

Cedar Mountain , 2011). Minor current , earthy facies, together in press

et al.

whereas sediments per Curtis sediments, - .

level variations and , as , which are , 2018;

- .

) sea the system Curtis , suggest It is proposedIt is

surfaces pal would was was . This is in press aeolian - marine marine a

tion - eosols (43) (

erns erns near Fig ), Fig. s -

This article isprotected rights by All copyright. reserved. grained matrix distally (Fig. 12) that promote development of conglomeratic channels and dunes at the time ofdeposition, compared to aspatial and temporal partitioning of energy levels al. expected within tidally dominated systems sedimento deposition of the middle and upper Curtis sediments. during deposition of thelower Curtis sediments were generally lower than those present during The sedimentology ofthe distribution, Facies energybasinlevels, geometry andtidalresonance 2012; Shaw Gowland, 2011; Roos accompanying the deposition of the middle Cur suggest Curtis Formation Curtis times is wellas the absence of thewithin neighbouring and c et al. rather than a dominant control upon sedimentary character 7 It is important to note that similar bedforms the sedimentology is subordinate. significant surfaces that represent marine regression, and the influence oftidal processes upon middle Curtis times. The upper Curtis sediments (FA6 localised tidal influence. interpreted the as wave represent a significantly higher effects of allocyclic controls upon the sediment influence is present within the shallowing upwards successions but it correlated by the flooding surfaces that bound them. The sedimentary signature oftidal represent early marine transgression of the Curtis marginal in study The sequence stratigraphic DISCUSSION short and superficial vegetation ) , 2002;

Accepteddo occur in otherdepos Article , 2016; - - related sedimentary structures lived marine terpret the -

Fan, 2012) marine setting with variable tidal influence. lowerThe Curtis sediments (FA2 logical trends displayed within the lower Curtis are counter onset oftidal resonance Gugliotta et al. difficult to

s

(Fig. 4

sediments ofthe Curtis , 2014). , coupled with

over transgressions. . They a imply generally consistent average energy level tow A & et al. printing ofallocyclic sedimentary signatures )

Schuttelaars, 2011; Longhitano . This may be explained by a t

Consequently, wave reconcile Curtis

it commonly , 2016).However, because ofthelack of any major fluvial

model forthe Entrada ional ional systems in which currents tidal act ontemporaneous Entrada Sandstone and Summerville Formation current indicators a energy environment

Formation semi

.

The is a

developed and surfaces of sequence - enclosed, elongated the

reasonable hypothesis near Formation

Curtis sea (Boyd suggests that energy levels within the Curtis to - exclusively ology. The middle Curtis sediments (FA5) tis the observedones in the Curtis Formation

where the , a -

et al. (Sztan Curtis sea sea

to be deposited in a shallow hypothesis ofa mixed

impacted impacted by idal reworkingidal within a confined basin of was However, the – in which , 1992; Dalrymple

et al. FA - ó

tida Summerville interval

in a oftidalstate resonance during &

8) display stratigraphically

system remained unflooded by basin configurationbasin

, 2012; Reynaud

de Boer’s, 1995; Martinius (Martinius l ly influenced deposits ofthe -

for the major energy jump stratigraphic three parasequences can be

tidal processes, but

distal to proximal by only is subordinate to

to those of &

et al. those normally - as a modulating factor

energy system for Gowland, 2011;

significance. & , 1992;

presented in the Dalrymple, at the time, - a m ards theards coast dominant and

within a finer arine to systems

Harris lack

the & – sea sea

FA This is (Fig. both

Baas these 4) et - ,

This article isprotected rights by All copyright. reserved. quarter of 2012; Gowland, 2011; Roos Adriatic Sea, the Persian Gulf Tidal resonance rotational centre ofthetidal wave remains unknown amphidromic system could have developed 167.5 km, which is close to thewidth pal coefficient (8.3651*10 w required basin width for an amphidromic system to develop ( m. approximat In the Curtis sediments, 1968): the average for the sedimentology observed. systemtidal km inlength, and at least 150 t As 1995; Yoshida the subdued nature ofthe pre onset of tidal resonance 2007) that developed towards the end of lower Curtis times. result of an thewithin more proximal parts ofthe system, The southwards parasequence P into distal areas, and regressive pulses are notable during the development of sediment short as 2016). et al influenced and confined basins, such the as Bay of Fundy (Li Similar gravel topebble al. thefrom neighbouring extra here here , 2001),and/or from

AcceptedThe Article a he dimensionshe of the s eolatitude after Hintze ., 2014),., the San Francisco Bay (Barnard -

basinally sourced flash flood deposits (Zuchuat Shaw

g Alternatively, conglomeritic channels and dunes may result from the influx ofa coarser Rossby

is the gravitational accelerat the tidal wavelength

ion for the optimal basin configuration (Godin, 1993; Sztanó

bedform et al. ( Sztan et al. Deformation Radius ( 3 (Zuchuat

can can develop within a semi increase , 2014 - lived regressive pulses brought material from ó , 2007) may serv

& thickness &

- deepest waters ofthe Curtis , uplifted 5 de Boer, 1995 )

uplifted highlands to the west (Thorman, 2011; Anderson, 2015).

Schuttelaars, 2011; Longhitano , if the length ofthe embayment approaches an odd multiple of bedform rad/ to cobble in

in emi

middle Curtis times. et al. &

energy s at s 35° latitude ,

Kowallis - - or the Bay of Fundy km in width, it is possible to transgression relief by time this (Godin, 1993; Sztan enclosed, fluvially

of thetallest features observed in the succession

( , 2018). Uncompahgre terraces to theeast (Otto

Godin, 1993; The water depth

thickness

sized conglomeratic bedforms are found in modern , and the presence of sandier and more homogeneous strata e to promote resonance. R

) ion ion (9.81 m/s

of

) could have developed

(

200 for agiven pal the Curtis

-

enclosed basin h 9

within the Curtis

) et al (after Vallis’ can can reach

) Sztan may

.

T The physical dimensions ofthe basin

he he solution starved

., 2006) or the bay of Brest (Gregoire

(

( sea

2 d Sztan

be linked also to tidal amplification sea ó

),

)

& and impossible to constrain d

et al. in tidalsystems can be determined from . a

The calculations

eo

in the areastudy

is theis water depth, and de Boer’s, 1995 3 to 4 m

et al.

ó

Curtis -

( latitude , such the as Gulf of California, the & , 2018), that may have originated

determine

2017

, 2012; Reynaud de Boer, 1995; Martinius

et al to that may provide an This This may sea sea & Sztan

equation (2) is , de Bo sea sea )

which gives a minimum ., 2014;., Shaw the proximal part ofthe basin

basin Coriolis coefficient equation; approximately ó reached

& er, 1995; Yoshida whether an a

, but the location of the be the pre ; Yoshida

de Boer impl & of

Picard, 1976; Scott approximately y approximately &

that the uppermost approximately et al., f

, Dalrymple,

1995): is theis Coriolis et al ( -

. h explanation indicates the cursor to the

an ) m ó

by (Allen 2014; Todd & , along with phidromic , 2007 , &

tidally et al de Boer,

as as a a et al.,

20 .,

) 800 :

-

,

25

et

This article isprotected rights by All copyright. reserved. (Dromart over realms to such sub deposition of system. Nevertheless, climat localised uplift episodes and associated thewithin basin ( parts ofthe Entrada However, s above oscillations and the arid marine or superficially vegetated palaeosol horizons, it thatseems relative base aeolian sequences would be required in order to determine shallow the exact nature ofrelative sea (Fig t Consequently, it may be suggested that wind transport, Pellenard a cooling event during the Upper Callovian Age Tethyan Ocean during the Callovian and Oxfordian ages, Both C level variations (Boulila which overprinted the stratigraphic sig the as middle and upper Curtis were being deposited, dominated was by autocyclic interactions, 2010 allocyclic, orbitally of the middle Curtis, theregional extent and abrupt nature ofwhich may be linked to an phenomenonThe ofresonance may have been triggered by the Major Transgression at the base provide some explanation for the variation the approximately approaches For subaqueous morphology ofthe However, Schuttelaars, 2011 where he lower he Curtis, the Moab Member ofthe Curtis Formation, and the Summerville Formation Accepted cyclcityauses of Article total length of the s water

whether the eccentricity cycles leadto small , 405 and 100 kyr, orbitally forced eccentricity cycles have been documented within 8 -

e 201 mentioned

L and

- adjustment

marine, supratidal, and aeolian deposits of the studied area and their equivalents local is the tidal wavelength, et al. such resonant behaviour et al. depth 1

hort 10 ; Strasser approximately

the lower Curtis ), may be related to one (or both) ofthese two Milankovitch , 2003; Wierzbowski , 2014). Such acooling episode, accompanied by increased sediment 156 - may may explain s lived episodes of

Fig d

eccentrici

), - of the Moab -

regional uplift events is difficult to km or forced, relative sea of in the continental, contemporaneous counterparts to the shallow - g s lower

et al. Curtis approximately multiple is theis gravitational acceleration (9.81 m/s 10 - et al. humid climat

and 175 , 2012; Pellenard

Curtis interval, which 625 ty cycles.

sea the growth and demise oftheEntrada aeolian system. , 2010, 11; ;

respectivelykm,

- the potential climat Member ofthe C s

level variations remains uncertain tidal km, km, , tidal resonance could have hort T Zuchuat sub

is the period of the M2 tide (44

depends et al. or 201 - system

- lived episode 20 m regional e - 700 km

natures of most level rise during the sedimentary variations relative sea 1 , 2009; Donnadieu

cycle periodcycle (or frequency). ; Strasser et al.

and 25 (equationm 1)

in sedimentology observed throughout Curtis times

et al. (Roos also upon tectonic uplift have accompanied deposition of respectively , 2018 . As these values (Boulila urtis Formation, each , 2014). The resultant tidally resonant system, may have - scale, glacio were e s & et al. -

of tectonic uplift occurred

response of thearid paralic and continental level oscillations

cycles recorded in the Entrada Sandstone, Schuttelaars, 2011; Wang ,

in fully the L

et al. responding simultaneously to , 2012; Pellenard press with ower Oxfordian, allocyclic relative sea

basal shear stress

, which impacted upon relative sea assess et al. L developed , 2010, ower Oxfor in which ) - eustatic sea . are I , 2011; Alberti 2 t seems unlikely ), and , the tidal wavelength ’ . Further 712 s , an gives a approximately 201

d p triggered a truncated by shallow Considering the δ within the basin econds d 18 1 recise dating ofthe dian (Boulila

O is the water depth ; Strasser

et al. - quarter wavelength of more - t isotopic data indicate level variations ype es ; , 2014).

during the et al.

and the et al.

Roos cycles. However, - , debate persis

level

simultaneous that

one fifth et al. available , 2014). , 2012; - & /sea marine marine et al. such five five

- the

level L

, 2012; and may

the - level , -

. of

for ts - .

This article isprotected rights by All copyright. reserved. deposits outside ofthe shallow overprinted by those of tidal currents, despite their presence in neighbouring thewithin Curtis correlatable stratigraphic surfaces Sediments ofthe middle Curtis unit by tidalprocesses. packages that are governed by allo causes levelsea that their marine erosion) are Major stratigraphic surfaces (flooding surfaces, ravinement surfaces, and regressive surfaces of post deposits ofthe Moab Membe of majortransgression. The middle and upper Curtis units earthy facies of contemporaneous with the lowerThe Curtis sediments represent early transgression of theCurtis elongate and influence from contemporary and neighbouring systems, and often arranged in cyclical bundles. tidal wellas cross dominance on deposition includes responded to allocyclicl deposited in a shallow The CONCLUSION approximately 0.9 and 3.6 Ma. 10 Consequently, as nine relative sea (Aurell variations within a Mesozoic greenhouse period, driven by 100 or 405 kyr eccentricity cyc decametre. This magnitude matches estimations of the amplitudes ofrelative sea incision at Sven’s amplitudeThe oftherelative sea Boulila of thermal Chumakov

Accepted Article), itis possible tobracket the time encapsulated wi

- sediments of the major transgression deposition. correlative

remain & et al.

Bádenas, 2004; Boulila water expansion and/or ground et al. , 201 shallow may be equivocal - the , 2014), or stratified and heterolithic sandstone withflaser bedding, both ofwhich are

continental 1 sea Gulch

). E

traceable . The signatures of allocyclic processes within the ntrada sandstone

connected Upper basin - marine to marginal

y controlled fluctuations in relative level.sea Evidence ofastrong tidal (9) ( . The sur whether whether , propitious to neighbouring Jurassic

Fig. 3E),suggests relative sea equivalents r

of the Curtis Formation through sediments of the lowe - marine to - et al. faces level variations also remains unconstrained. However, tidal - . level cyclic process,cyclic 100 and or 405 kyr bi

T these sea are characterised exclusively by tidalfacies an

Curtis - he

directional ripple cross , 2010 . lowerThe divide y represent realm Tidal dominance is emphasised by a of fluviallack cycles . Th

wet i an efficient dissipation of wave energy - - F marine, tidally dominated environment that water recharge (Schulz , ese ormation of the

-

201 . the sedimentary succession into anumber of level variations a

were recorded within the Curtis Formation (Fig. nterdune to coastal sabkha sed

surfaces are related to 1

but display internal sedimentology dominated - ; Strasser

the onset oftidal amplification by middle Curtis boundary represents the onset thin thethin Curtis Formation to between

and Milankovitch - , level variations of theorder of one Summerville

along with the et al. Colorado Plateau, Utah, USA, were - r Curtis,

stratified silt a lack of wave influence within the re dueto orbitally , 2012; Pellenard & cycles,

and Schäfer sediments oscillations sea

Formation

upper Curtis contemporaneous stone and

and are generally although the exact - iments of Neth, 1997; contemporaneous .

-

- are forced level

d a lack d a lack of , et al. in relative

represent

sandstone, resonance , and

, 2014).

the

cycles les

,

This article isprotected rights by All copyright. reserved. J.H. Special Papers Laurasia the Mexico Anderson, T.H. 182. Allen, J.R.L. reconstructions. potential for palaeoecologic, palaeoclimatic, and palaeogeographic δ Alberti, M., Fürsich, F.T., Wonham, J.) Norwegianthe continenta Jameson Land development in a tide Ahokas, J.M.,Nystuen, J.P., REFERENCES There areno conflicts of interest in the preparation or publication of this work. Conflict of Interest acknowledged for their constructive observations and remarks. anonymous r publishedis by permission ofthe Executive Director, British Geological Survey (UKRI). for their assistance and fruitful comments, which enhanced the quality ofthis work. Dr Anja Sundal awarded COPASS grant 244049. Acknowledgements are to be extended to authorsThe of this paper would lik Acknowledgements embayment environments, particularly in wheresettings the marine basin forms a small and marine strata in the context of autocyclic processes of the marine system, such tides. as sea normally dominant The demonstratesstudy that, given the right sedimentary basin 13

AcceptedC) ofbelemnites, brachiopods, and Article - ) level

,

513 – oscillations , 107

A Record F of - Alaska megashear, from the Gulf of Mexico to Alaska. , is clear

, (1968). natureThe and origin of bed

eviewers IAS Special Publication,

Basin, East Greenland. ( - ,

188. E

Dr Miquel Poyatos

(2015). Jurassic (170 Palaeogeography, Palaeoclimatology, Palaeoecology ds

Anderson, T.H., Didenko, Johnson, A.N., C.L., Khanchuk, A.I., and MacDonald, allocyclic signatures within shallow

.

may be overprinted and obscured by the usually subordinate localised - influenced marginal marine basin: Early Jurassic Neill Klinter Group, who worked on an earlier aulting Accommodatingaulting Plate Rotation l margin

and

and Pandey, D.K. the Martinius, A.W.

( - deposits e to thank the Norwegian Research Council fortheir Moré, E ds 46 In – oysters from the Kachchh Basin (western India) and its 150 Ma) basins: The tracks of acontinental

, 291 : Martinius, A.W.,Ravnas, R.,Howell, J., R.J.,Steel, & From depositional systems sedimentary to successions on

Dr

of

- Mark Mulrooney, (2012). Oxfordian The isotopestable record (δ 338. their neighbouring and ‐

version

(2014). Depositional dynamics and sequence form hierarchies. - marine sediments

T of this ma he importancehe of

. Anna v. Yperen

Geological Society ofAmerica

geometry In : nuscript Late Jurassic Margin of ,

Sedimentology 344 contemporaneous , 49

and conditions, the Dr Hannah L. Brooks r

examining elated to relative are to be sincerely - , and CoteNathan 68.

protected

- scale fault, ,

The paper 10

The threeThe sha , 161

llow

18 - O, -

, This article isprotected rights by All copyright. reserved. t Bump, A.P. p. 15952. and interpretation of virtual geoscience models. Buckley, S., Ringdal, K., Dolva, B., Information measures for terrain visualization. Bonaventura, X., Sima, A.A., Feixas, M., Buckley, S.J., Sbert, M., for Se (Eds of theWestern Interior Seaway, USA. Brenner, R.L. environments. Boyd, R., Reviews (2011). On the origin of Cenozoic and Mesozoic “third Boulila, S.,Galbrun, B.,Miller, K.G., Pekar,Browning, S.F., J.V., Laskar, J., noires formation France)(SE and global implications. D. Boulila, S.,Galbrun, B.,Hinnov, L.A., Collin, P.Y., Ogg, J.G., Fortwengler, D., Bostock, J., North Sea. dynamics in semi de Boer, W.P., Roos, P.C., Hulscher, S.J., 962 in a retroa Bjerrum, C.J. stratification in cohesive mixtures of mud and sand. Baas, J.H., Best, J.L., mouth of San Francisco Bay. Barnard, P.L., Hanes, D.M., Rubin, D.M., Spain). high Aurell, M., RockyThe Moun Systems the Rockyof Mountain Region paleogeography in the southern Colorado Plateau and southern High Plains. Anderson, O.J. he northernhe Colorado Plateau, Utah and Colorado.

Accepted(2010). Milankovitch and sub Article - - 978. Caputo, M.V., Peterson, J.A. and Franczyk, K.J.), RockyThe Mountain Section SEPM (Society frequency sea dimentary Geology), Denver, 233

Geological Magazine ,

109

Dalrymple, R.,

rc foreland basin, Utah

Coastal Engineering Proceedings and

and and , 94

and

and Sedimentary Geology

and Bádenas, B. Riley, H.T. Davis, G.H. - tain Section SEPM (Society for Sedimentary Geology), Denver, 299 - 112. enclosed basins: The effects ofa mega Dorsey, R.J. Peterson, J.A. - Lucas, S.G. level changes in a shallow

and

Peakall, J. and

(1855). Pliny the Elder. ,

(2003). Late Cretaceous

(2004). Facies and depositional sequence evolution controlled by Eos, Transactions American Geophysical Union 141 Zaitlin, B.A.

(1995) Tectonic controls on deposition of Middle Jurassic strata (1994). MiddleJurassic stratigraphy, sedimentation and - , 717 Milankovitch forcing ofthe Oxfordian (Late Jurassic) terres ‐ (1994). Jurassic sedimentary history ofthe northern portion Idaho trough, western interior, United States. Naumann, N.,

, (2016). Predicting bedforms and primary current

80 In , USA - 733. - , 139 : 272.

Mesozoic Systems the Rockyof Mountain Region, USA

and and

(1992). Classification of clastic coastal depositional (Eds (Eds ,

1

- 150. , 1 - Stolk, A. Kvitek, R.G. water carbonate ramp (late Kimmeridgian, NE

Computers Geosciences& - Caputo, M.V., Peterson, J.A. and Franczyk, K.J.), EGU General Assembly Conference Abstracts 7.

and

Journal ofStructural Geology The NaturalThe History Journal of the Geological Society – -

Basi early Tertiary Laramide deformation of

order” eustatic sequences. Kurz, T. (2011). An idealized model tidal of - scale extractionsand trench in the n Research

(2006). Giant sand waves at the

(2017). LIME: 3D visualisation

and , 22 Howell, J.A. ,

16:1 , , 717

99 ,

87

, 9 In and (2). -

, and 732. - :

285 18. Mesozoic Mesozoic ,

25

Wright, J.D. Tectonics Earth

Marchand, (2017).

- - , 421 289. 314. , 173 - Science

- , 12 440. ,

, 14

19 -

45.

, ,

This article isprotected rights by All copyright. reserved. USA. paleotectonics from U Dickinson, W. intraregional recycling ofsediment. associated sandstones ofthe Colorado Plateau Dickinson, W.R., implications. Jurassic eolian sandsto Dickinson, W.R., and stratigraphic implications: perspective. Dalrymple, R.W., Zaitlin, B.A., Survey Bulletin Wanakah Formation, northwestern NewMexico and northeastern Arizona. Condon, S.M., Geological Society Special Publications, In Crabaugh, M., and Geological Correlati al.(2011)“A mechanism for brief glacial episodes in the Mesozoic greenhouse”). at theAsia Middle Chumakov, Edgar,C.B., N.T.), stratigraphy, emphasizing the climatic variable. Cecil, C.B. 59 system: a key to relative sea Carr Earth Tucker, M.E., Pomar, L., Posamentier, H.W.,Pratt, B.R., Sarg, Shanley, J.F., K.W., Steel, R.J., Strasser, A., R., Kendall, C.G.St.C, Macurda, B., M Fielding, C.R., Fisher, W.L., Galloway, W.E., Gibling, M.R., Giles, K.A., Holbrook, J.M., Jordan, Catuneanu, O., Abreu, V., Bhattacharya, J.P., M.D., Blum, Dalrymple, R.W., Eriksson, P.G., Catuneanu O. 27. and paleography, upper San Group,Rafael east Caputo, M.V. sequence stratigraphic interpretations. Burgess, P.M., :

Accepted Article, 213

The dynamicsThe and environmental context eolian of sedimentary systems - International Journal ofEarth Sciences Crabaugh, M. - Science - 228.

( 2003

N.M., Zakharov, V.A.,

Sedimentary Geology and

Reviews and

and R.,

, (2006). and and

1633 )

. The concept of and and and - Pryor,W.A. SEPM (Society for Sedimentary Geology) Winker, C. Late Jurassic boundary? (Critical remarks on the article by Y. Donnadieu et Huffman Jr, A.C. Kocurek, G.

Prince, G.D. and - , – A Gehrels, G.E. Gehrels, G.E. Gehrels, G.E. Principles Sequenceof Stratigraphy nes ofthe Colorado Plateau, USA: paleogeographic 92 Pb ages ofdetrital zircons in Mesozoic strata of the Colorado Plateau, , A1 on Kocurek, G. , 1 ,

22 - - - A12. 33. level change.

, 655 (2009). Towards the standardization of sequence stratigraphy. (1991). Middle Jurassic tide

and

(1993). Entrada Sandstone (2015). Non

autocyclic and allocyclic controls on sedimentation and ,

and - 163

658.

(2010). Insights into AmericanNorth paleogeography and (2009). U (2003). U Boyd, R Geological Society Americaof Bulletin (1988). Revisions in nomenclature of the middle Jurassic

(1998). Continental sequence stratigraphy of awet eolian artinsen, O.J.,Mial, A.D., Neal, J.E.,Nummedal, D.,

72 Rogov, M.A.

, 29 Basin Research

, 103

Society for Sedimentary Special Geology, Publication, - ,

66. Journal ofSedimentary Research 99 . - (1992). Estuarine facies models: conceptual basis unique geometries: stratal implications for - – — Pb ages ofdetrital zircons in Jurassic eolian and - -

Pb ages ofdetrital zircons from Permian and , 1247 126. central Utah. In evidence for transcontinental dispersal and : Climate Controls on Stratigraphy

(2014). Did an ice sheet exist in Northeast - 1265. ,

27

. Special Publication , 351 - Amsterdam, Elsevier, 375

—

and wave Utah Geological Association, an example ofa wet eolian system. - 365.

- influenced coastal facies

, (Eds (Eds 121

U.S. Geological ,

, 62 77 , 408 Pye, K.),

, 1130 Stratigraphy , 13 -

- 433. (Eds (Eds

20. pp. - 1146.

London

.

19 Cecil, , 9

- This article isprotected rights by All copyright. reserved. AcceptedNorwegian continental shelf I.M., Halland, E.K., deposits (Lajas Formation, Argentina). characte Gugliotta, M., Flint, S.S.,Hodgson, D.M., France). sedimentological patterns in a tide Gregoire, G., Ehrhold, A.,LeRoy, P., Jouet, G., Godin, G. adjacent areas in eastern Utah. Gilluly, J. tracemaker. Getty, P.R. in evaluation of clay minerals. Fertl, W.H., Chilingarian, G.V., and Dalrymple, R.W.), Fan, D. age at the Middle ArticleDromart, G., Garcia, J.P.,Picard, S., Atrops, Lécuyer, F., C., Entrada Sandstone in central Utah Dossett, T. S. greenhouse. Olivier, N. Donnadieu, Y., Dromart, G., Goddéris, Y., Pucéat, E., Brigaud, B., Dera,Dumas, G., C., 267DM, scale 1:62,500. Desert x 60' 30' quadrangle, Emery and Grand Counties, Utah Doelling, H.H., Kuehne, P.A., Willis, G.C., Ressetar, R.) San Rafael and Swell Henry Mountains Basin Carmel Formations in the Henry Mountains Basin, Wayne and Garfield Counties, Utah. Doelling, H.H., Sprinkel, D.A., Kowallis, B.J., Survey Map 180, 3plates, scale 1:100,000. quadrangles,60' Grand and Emery Counties, Utah, and Mesa County, Colorado Doelling, H.H.

Mujezinović, J.,

(2012). Open

ristics and implications ofthe fluvial tomarine transition zone in ancient deltaic Journal of Maps

and (1993). On tidal resonance.

(2011). A mechanism for brief glacial episodes in the Mesozoic and

, Palaeontology Paleoceanography and Paleoclimatology

Utah Geologica (2014). Reeside Jr.,Reeside J.B.

Bjørnestad, A., Magnus, C., Riis, F., Meling, I.M., Tørneng Gjeldvik, I., Tappel, (2001). Hagadorn, J.W. – Late Jurassic transition?. - Bjørheim M., Rød, R.S.,

coast flats.tidal The The f Dordrecht, Netherlands, Geologic map ofthe Moab and eastern part the San of DesertRafael x 30'

,

12 , irst 40Ar/39Ar ages and tephrochronologic framework forthe Jurassic

52 . Stavanger, Norway, Norwegian Petroleum Directorate. , 1152 l Associationl Publication

, 753 Energy Sources (1928). Sedimentary rocks of the San Rafael Swell and some U.S. Geological Survey, Professional Paper ,

and (2009). Palaeobiology ofthe Climactichnites . -

- Brigham Young University 1159. - dominated estuary system: the Bay of Brest (west Britanny, 778. Yen, T.F. Yen,

Continental Shelf Research In

Sedimentology :

Principles tidalsedimentologyof and

and

Earth and Planetary Science Letters - geologic centerpiece Utah of

,

(1982). Use of natural gamma ray spectral logging Veiga, G.D. and and 6 Ehler, J.B. Springer and Science Business Media

and (4), 335 Pham, V.T.H. Kuehne, P.A. (2013) Garlan, T. , ,

42 , 26

63 - , 279 , 1 360.

, 1971 (2015). (2016). Recognition criteria, -

10. . Utah Geological. Utah Survey, Map

and

- , Utah 318.

(2016). Modern morpho -

, 2001. (2014).

13 Sheppard, S.M.F. Geologic map San ofthe Rafael

, master thesis , 89

- . Temple Cap and

107. CO (Eds 1

(Eds 50 2

. GeologicalUtah storage atlas

- Morris, and T.H., D , Davis, R.A., Jr.,

213 ,

61 ,

1

- (2003). Ice

, 205 - 110. , 187 46. In -

: - and –

— 220. The The 229.

This article isprotected rights by All copyright. reserved. 381 sedimentary structures of the Curtis Formation, Utah. Kreisa, R.D. Mexico, USA. evapor Nazworth, C.M. Mason, J., Cardenas, B.T., Petersen, E., Mohrig, D., Aylward, D.S.,Hughes, C.M., Kocurek, G., Desert Kelso dune field example. Kocurek, G. and In Kocurek, G. (Eds Sandstone examples. Kocurek, G. surfaces revi Kocurek, G. continental setting. Imlay, R.W. Association Petroleumof GeologistsBulletin Imlay, R. W. Association Petroleumof GeologistsBulletin Imlay, R.W. University Studies. 225pp. Hintze, L.F. sheets. L.F. Hintze, Uplif Utah. eastern and Colorado western Uplift, Uncompahgre O., Heyman, Triassic. Haq, B.U., Hardenbol, J., analysis ofwave, tidal, and river power. Classification of Australian clastic coastal depositional environments based upon a quantitative Harris, P.T., Heap, A.D.,Bryce, S.M., Porter :

Accepted Article Siliciclastic Sequence Stratigraphy: Recent Developments and Applications

- t Posamentier, H.W.) 387. Chan, M.A., (Eds (Eds

ite facies: Middle Jurassic Todilto Member, Wanakah Formation, Ghost Ranch, New

Science

Averett, W.), Grand Junction Geological Society, Grand Junction, Colorado, 45 Colorado, Junction, Grand Society, Geological Grand Junction Averett, W.),

and

(1980). (1980). Jurassic paleobiogeography of the conterminous United States in its (1947). Marine Jurassic ofBlack Hills Area, South Dakota and Wyoming. and and ( (1988). First sited. and (1952). Marine origin ofPreuss sandstone of Idah Sedimentology Martindale, R.C., Day, M., Goudge, T.A., Kerans, C., Hassenruck (1983). Distribution and structural geometry of faults and folds along the northwestern northwestern the along folds and faults of geometry structural and Distribution (1983). 2003

, and (

Kow Lancaster, N. Havholm, K.G. 235 Moiola, R.J. 2018

Sedimentary Geology )

Geologic map of Utah. of map Geologic U.S. Geological Survey Professional Paper . Limits on extreme eolian systems: Shara of Mauritania and Jurassic Navajo Archer, , 1156 In allis, B.J. ). Antecedent aeolian dune topographic control on carbonate and :

, Extreme depositional environments: mega end members in geologic time American Association Petroleumof Geologists, Memoir,

- and order and super bounding surfaces in eolian sequences

- , 1

1167. A.W.),

(1986). Sigmoidal tidal bundlesand other tide Vail, P.R. -

30

(2009). (1999). Aeolian system sediment state: theory and Mojave

(1993). Eolian sequence stratigraphy: A conceptual framework.

Sedimentology .

Geological Society ofAmerica Special Paper Geologic history ofUtah.

,

(1987). Chronology offluctuating sea levels since the

Journal Sedimentaryof Research 56

Utah Geological and Mineral Survey, scale 1:250,000, 2 1:250,000, scale Survey, Mineral and Geological Utah , , , 193

31 36 - Smith, R., Ryan, D.A., , 227 , 1735 , -

46 206. , 505 - 273. -

1753. Geological Society Americaof Bulletin In -

515. :

Northern Paradox Basin Paradox Northern

, 1062

o, o, Wyoming, and Utah. Provo, BrUtah, , 1

and - 134. , Heggie, D.T.

72

-

, 858 , (Eds (Eds generated , igham Young 370 ‐ 58 - Weimer, P., — Gudipati, H.J., 870.

, 393 - and Uncompahgre Uncompahgre , 43 bounding American

- (2002). American

57. - – 52. 410.

,

97

,

This article isprotected rights by All copyright. reserved. Mountains. Acceptedthe central Colorado Plateau documented by apatite thermochronology the from Henry Murray, K.E., Reiners, P.W., interdune successions. Mountney, N.P. 823. Permian Cedar Mesa Sandstone, White Canyon, southern Utah, USA. Mountney, N.P. Hydrocarbon Exploration unit for stratigraphic analysis. Mitchum, R.J., Vail, P.R., in an epicontinental thesea: lower Cretaceous of Svalbard. Midtkandal, I., Bighorn Basin, Wyoming, USA. invertebrate fossils in a sequence stratigraphic context: the Jurassic Sundance Formation, McMullen, S.K., Holland, S.M., Norway. Reservoir challenges of heterolithic tidal sandstone reservoirs in the Hal Martinius, A.W., Ringrose, P.S., Brostrøm, C., Elfenbein, C., Næss, A., Portugal). deposits (late Jurassic Martinius, A.W. Articleof southeastern Idaho. Mansfield, G.R. Jurassica Mountains, southeastern Utah: Stratigraphic relationships ofthe Bluff Sandstone. Lucas, S.G. systems in the rock record: a review and new insights. Longhitano, S.G., Mellere, D., Steel, R.J., Canada. development ofbanner banks and sandwaves Li, M.Z., Shaw, J., Todd, B.J., Kostylev, V.E., lithospheric downwelling. Humphreys, E.D. Levander, A., Schmandt, B., Miller, M.S., Liu, K., Karlstrom, K.E., Crow, R.S., Lee, C. Dalrymple, R.W.), recognition and analyses. Kvale, E.P.

Continental Shelf Research , Petroleum Geoscience 12

Sedimentology

(2014). Lithostratigraphy of the Jurassic San GroupRafael from Bluff to the Abajo (2012). Tidal constituents of modern and tidalancient rhythmites: criteria for Geology , 55

and

- and (2012). A stratigraphic model toaccount for complexity in aeolian dun (2006). Periodic accumulation and destruction of aeolian erg sequences in the and 68.

S (2011). Continuing Colorado plateau uplift by delamination pringer Science and Business Media ,

Nystuen, J.P. 44 Roundy, Roundy,

Gowland, S. Lourinhã Formation, Lusitanian Basin, Western

U.S. Geological Survey Professional Paper , Sedimentology

483 , ,

and 58 In American Association Petroleumof Geologists Memoir,

Nature : -

, 285 486. Principles Tidalof Sedimentology and Thompson, S. III. P.V. ,

In: Palaios 11 and

, -

Payton, C.E. Thomson, S.N. (2009). Depositional architecture ofa

, 3

(2011). Tide 324. , 472 (1916). Revision ofthe Beckwith and Bear River Formations

83 O'Keefe, F.R.O'Keefe, - 16. , , , 86 59 ,

29 461

, and -

, 277 964 107. - and 465. , (ed.),

Ainsworth, R.B. in an extreme tidal system: Upper Bay ofFundy, - ‐ -

989. 294.

(1977) The depositional sequence as a basic Wu, Wu, Y.

influenced fluvial bedforms and tidalbore

(2016). Rapid(2016). Pliocene (2014). The occurrence ofvertebrate and

Seismic Stratigraphy: Applications to

Sedimentary ,

(2014). Sediment transport and Dordrecht, Netherlands,

Basin Research

( Eds

(2012). Tidal depositional , 98 , 75 Geology

Davis, R.A., Jr., and Sedimentology, - 84. and low – ten Terrace, mid Pleistocene erosion of ,

21 ,

-

Ringås, J.E.Ringås, 279 gradient ramp shelf , 655 - style convective

26 , 2 1 Volumina - , 205 - 17. -

675. 53 22. -

, 789 T.A.,

e and -

(2005). 212. - - and

This article isprotected rights by All copyright. reserved. seascape maps of theBay of Fundy, Canada. Shaw, J., Todd, B.J., Mesa County, Colorado and Scott, R.B., Harding, A.E., Hood, W.C., Cole, R.D., Livaccari, R.F., J 231. eustatic fluctuations via thermal deep water expansion: a conceptual link. Schulz, M., amplification in semi Roos, P.C. Media Tidal Sedimentology Reynaud, J.Y. 1035 Formation in southeastern and Idaho adjoining areas. Pipiringos, G.N., Paper, rocks, western interior United States: a preliminary survey. Pipiringos, G.N. Professional Paper JurassicMiddle formations, southern Utah and northern Arizona P SEPM (Society for Sedimentary Geology), Denver, 233 Region, USA the southern part of the Western Interior Basin. Peterson, F. transition, eastern Paris Basin(France). (2014). Carbon cycle and sea Pellenard, P., Tramoy, R., Pucéat, E., Huret, E., M., Martinez, Bruneau, L., Petroleum Geologists Guidebook, 231 Utah. Otto, E.P. controls. Osleger, D. (1991). Subtidal carbonate cycles: Implications for allocyclic vs. autocyclic Ogg, J.G., Ogg, G., age determination. Nelson, S.T. Accepted eterson, F. Article

Dickerson, R.P.

- In , C

1035 Dordrecht, Netherlands, , 1 : J.G., Hill, (ed),

Geology - and and 25. and

(Eds (Eds -

(1997). Reevaluation of the Central Colorado plateau laccoliths in the light of new A and (1994). Sand dunes, sabkhas, streams, and shallow seas: Jurassic pal

and Picard, M.D.

, 1 Schuttelaars, H.M.

Schäfer

- and , Caputo, M.V., Peterson, J.A. and Franczyk, K.J.), The Rocky Mountain Section Pipiringos, G.N. and

29. and 19

, Dalrymple, R.W.

1035 U.S. Geological Survey Bulletin

and

(Eds (Eds

(

(2001). - O’Sullivan, R.B.

Imlay, R.W. , 917 enclosed basins. Gradstein, FM. . U.S. Geological Map I Geology ofthe Cordilleran hingeline. ‐

Li, M.Z. Li, - Davis, R.A., Jr., B Neth, C. - , 1

920. (1976). Petrology ofthe Entrada Sandstone (Jurassic), northeastern - Geologic map ofColorado National Monument and adjacent areas, - water palaeotemperature evolution at the Middle 43.

335

(2014). Geologic insights from multibeam bathymetry and

(1979).

(1979). Lithology and subdivisions of theJu (2011). Influence oftopography on propagationtide and (1997). Translating Milankovitch climate forcing into -

369. (2012). Shallow

- (1978). Principal unconformities in Triassic and Jurassic

259. Ocean Dynamics (2016).

and Dalrymple, R.W.), Marine and Petroleum Geology

Stratigraphic relations of the Navajo Sandstone to

- Continental Shelf Research 2740, 40 p., 1 plate, scale 1:24,000.

A Concise Geologic Time Scale: 2016 In ,

2158 :

Mesozoic SystemsMesozoic the of MountainRocky - marine tidal deposits. - U.S. Geological Survey Professional Paper, 272. ,

, 37 61

, 21 Rocky Mountain Association of

- U.S. Geological Survey, Professional 3 9.

- Springer Science and Business 38.

. U.S. Geological Survey

ohnson, J.B., Shroba, R.R., , ,

83 53

, 53 Terra Nova , 30 In and - : - rassic Stump

63. 43. Principles of –

Late Jurassic

Thierry, J. eography in

.

Elsevier. ,

9 , 228

- This article isprotected rights by All copyright. reserved. AcceptedBrigham Young University, Utah, master thesis, 1 and Regional Implications ofInterfingered Sabkha and Fluvial Terminal Splay Sediments. Valenza, J.M. Research evaporite deposition, salt wall growth and supra Trudgill, B.D. ResearchShelf sedimentary bedforms in a macrotidal setting: The Bay ofFundy, Atlantic Canada. Todd, B.J., Shaw, J., Li, M.Z., Kostylev, V.E., Yonkee, W.A.,and Chidsey, T.C., Jr.), Utah. Thorman, C.H. shorelines of theSauk epicontinental sea. Sandstone (Upper Cambrian), southeastern Minnesota, USA: evidence fortides along inboard Tape, C.H., Cowan, C.A., 665 amplification of tidal motions (theEarly Miocene North Hungarian Bay). Sztanó, O. in continental sequences. logging and rockwhole geochemistry: Implications for quantitative reservoir characterisation Svendsen, J.B. Young University Geology StudiesArticlesoutheastern Utah Sullivan, K.R., Kowallis, B.J., Mountains). changes on a shallow carbonate platform (Late Oxfordian, Swiss Jura Strasser, A., Vedrine, S., analysis. shallow carbonate Strasser, A., B., Pittet, Hillgärtner, H., Association Publication Adjacent Areas Sandstone and Glen Canyon Group, Utah. Sprinkel, D.A., Kowallis,B.J., Chidsey, T.C., Jr.), Thrust Belt: Northern andCentral Utah and Adjacent Areas results of a study of M Sprinkel, D.A., Doelling, H.H., Kowallis, B.J., Waanders, G., - 682. In :

, Sevier Thrust Belt: Northern and Central Utah and Adjacent Areas

Sedimentary

23 and

Sedimentology , 208

(2016). Redbeds ofthe Upper Entrada Sandstone, Ce

, (2011). Evolution of salt structures in the northern Paradox Basin: Controls on

(Eds (Eds 83 de Boer, P.L. and

(2011). The Elko

- Utah Geological Association, Publication, , 64 238. - –

dominated sedimentary systems: concepts for a high Hartley, N.R.

Sprinkel, D.A.,Yonkee, and W.A., Chidsey, T.C., Jr Evidence for a mid - Geology iddle Jurassic strata in the Sevier fold and thrust belt, Utah. 85.

, 40 and

and Marine and Petroleum Geology , 131 ,

59

(1995). B Runkel, A.C.

, Stienne, N. and

and , 185 128 - 149. ,

orogeny (2001). Comparison between outcrop 37

Mehnert, H.H.Mehnert,

Jensen, P.H. , 201

- Utah Geological Association Publication, , 139 211.

asin dimensions and morphology as controls on - and - Cenozoic Reno 221.

-

In (2012). Rate and synchronicity of environmental Journal of Sedimentary Research – 144.

(2003). Tidal

:

A major tectonic event in eastern Nevada Pasquier, J. B.

and Sevier Thrust Belt: Northern andCentral Utah and

(2011b). Correlation and age oftheNugget

‐ Wu, Wu, Y. -

(1991). Isotopic ages of igneous intrusions in 54. salt stratigraphic architecture.

–

- (2014). Distribution of subtidal San San Juan magmatic zone. , bundle sequences in the Jordan

18

40 (Eds (Eds

(1999). Depositional sequences in , 657 , 151 and Sprinkel, D.A., Yonkee, W.A.,and -

670. Kuehne, P.A. - 172. ntral Utah: Facies Analysis .),

Utah Geological

- - spectral gamma ray

resolution Sedimentology

, (Eds (Eds

73 40 , 354 , 117 Sprinkel, D.A.,

(2011

Brigham In

Basin Continental - 366. : -

129. Sevier – a western ). Early ,

42

, This article isprotected rights by All copyright. reserved. AcceptedSedimentary Research Settings: the J A., Zuchuat, V., Midtkandal, I., Poyatos Intermountain West epicontinental basin (2018) Zuchuat, V., Sleveland, A.R.N., Sprinkel, D.A., Rimkus, A., Braathen, A., Research ingredient in a new generation of sequence Yoshida, S., Steel, R.J., the North American Cordillera orogenic system. Yonkee, W.A. Palaeoclimatology, Palaeoecology central Poland: A record of aLate Callovian global sea composition of Callovian Wierzbowski, H., Dembicz, K., 1764, scale 1:100,000. and Uintah Counties, Utah. Witkind, I.J. Association of Geologists and Utah Geological Association Publication, ArticleProduction in Uintathe Basin, Utah and Stump Formations, Easter Wilcox, W.T. applications. ‘Structure Westoby, M.J., Brasington, J., Glasser, N.F., Hambrey, M.J., Canada and James, N.P. (eds.), Walker, R.G. and East China Sea. Wang, D., Liu, Q., Business Media Principles Tidalof Sedimentology Wang, P. (2012). Principles ofSediment Transport Applicable in Tidal Environments. pp. Vallis, G.K.

and . New insights on the impact of tidal currents on a low Braathen, A. , 1 , - 77 - 14. from

(2017).

, 447

(1988).

Geomorphology

- (1992). Facies, facies models and modern stratigraphic concepts. and 3 Unconformity and the Curtis Formation, East and , -

Motion’photogrammetry: A low Dordrecht, Netherlands,

- Currie,B. and

460. Weil

, Mathematical Problems in Engineering Atmospheric and oceanic fluid dynamics —

5 Geol ( .

in press , 131

Facies models: response to sea Lv, Lv, X.

the Curtis Formation, east

and and , A.B. – ogic mapogic ofthe Huntington X 30' quadrangle,60' Carbon, Emery, Grand, Lower Oxfordian (Middle

U.S. GeologicalU.S. Survey, Miscellaneous Investigations Series Map I - Dalrymple, R.W. 165.

(2014). A study on bottom friction coefficient in the Bohai, Yellow, (2008). Sequence Stratigraphy ofthe Jurassic Curtis, Summerville, ,

(2015). Tectonic evolution of the Sevier and Laramide belts within 179 ). Composite Unconformities in Low n Utah and Northwest Colorado. and

(Eds ,

, 300 283

(Eds (Eds

Praszkier, T. - Davis, R.A., Jr., and Dalrymple, R.W.), Moré, M.,Costa, da S., , 182 - 314. Longman, M.W. 19 - - -

stratigraphic models. 194. 34.

(2007). Changes in depositional processes

- Earth

- cost, effective toolfor geoscience central Utah, USA (2009). Oxygen(2009). and – - Upper Jurassic) belemnite rostra from level changelevel - - level rise? Science Reviews ,

and Morgan, C.D.), ,

2014, 1 . Cambridge University - and - Halvorsen, N., K.,Cote Sundal, gradient, semi Central Utah, USA. In

,

Palaeogeography, : Reynolds, J.M. Geological Association of

Journal ofSedimentary - Hydrocarbon Systems and - Gradient Transitional . 7.

Geology of the 37

,

carbon isotope 150 , 9 - and 41.

Springer Science and Rocky Mountain , 531 - enclosed,

Midtkandal, I. In

- (2012). The Journal of : Walker 593. Press. In

: —

745 , R.G., an -

This article isprotected rights by All copyright. reserved. Accepteddisplaying regular episodes of marine flooding (white sandstone beds). the Moab Member of the Curtis Formation. FA 8 supratidal deposits of theSummerville Formation. and finer the underlying FA 5 black line on the diagram illustrates the outcrop orientation. migration direction of these three bedforms is colo contour) within a sub and blue contours), and a third south deposited. the collapse ofFA 3b deposits, as FA 4a sand of aregressive and erosive, subtidal channel complex (FA 4b). deposits during the tr a within matrix ofFA 3b sand phase within Parasequence 2. darkThe (FA 3b). stacking architecture ofsubtidal mu drapes. Note theloaded and eroded irregular geometry ofthe J scale. FA1b (Entrada Sandstone). Notethe bleached horizon direct Amalgamated aeolian coastal dunes within the fine ofExample Fig. 3 Formation. Table 2 ArticleFormation. Table 1 Member, and Summerville Formation is not shown in this lithostratigraphic display. Sandstone and the lower Curtis, as well as between the middle Zuchuat Ranch, in northern New Mexico ( column showing a correlation between the San Rafael area, Swell east River, HKS: Hanksville, MB: Moab, SRS: San Rafael Swell. 2015; Tectonic setting after Heyman, 1983; Thorman, 2011). GJ: Grand Junction, GR: Green 1988; Doelling, 2001; refers to aspecific locality in the attached table ( Formation crops out, while thered d Fig. 2 Harris Fig. 1 FIGURE CAPTIONS . . . (

( Modern day, tide Summary panel of the Facies Associations (FA) cropping outwithin the study area. C et al. A . . )

( et al., Facies associations for the Entrada S Facies description for the Entrada Sandstone, Curtis Formation, and Summerville - - E High grained FA 6 upper sub B ) (

) , 2002; wet coastal aeolian dunes of FA 1a (Entrada Sandstone, Slick Rock Member).

G

M Maps oftheMaps st )

ajor incision tidal observed at S - 2018;). Note thatthe contemporaneous character between the Entrada Two Two incision phases ofFA 4b subtidal channel. energy upper shoreface t Fan, 2012). s ub

tidal ansgressive phase of Parasequence 3, followed by the by the development Doelling

- tidal dominated coastline

to intertidal flatsurrounding environm udy Greenarea. representdots visited localities where the Curtis

to intertidal channel -

dominated deposits. also Note the ravinement of Parasequence 2 et al. Doelling, 2001; Doelling tidal , 2013; d ots illustrate its absence. Each code number on the map - -

westward laterally accreting tidal channel (green

to intertidal deposits, which are conformably overlain by (FA 3a) and sand - red arrow at points a boulder of Entrada Sandstone o beach deposits, with rip

Sprinkel ( K -

rich sub environments andstone, Curtis Formation, and Summerville ) ven’s Gulch, carved during a short

Close Geological units after Hintze, 1980; Witkind, - dune u - grained, marginal marine earthy facies of et al. r - - up images of FA 8 supratidal deposits tidal coded on the rose - - ( flat complex, grading into the thinner dominated heterolithic flat deposits , 2011a; 2011b; ( J et al. ) C

to supratidal sandflat bewas

) Five aeolian sequences recorded in

(modified from Schematic lithostratigraphic ly ( I ( , 2015; ( ) H - below Curtis, upper Curtis, Moab F

3 Unconformity. Conformable contact between ) )

Bidirectional tidalinlets (red - ent (FA 5). The respective Mini sag basinMini generated by up c

the dunes. Geologist for Kocurek - centra lasts and occasional mud

- diagram, whereas the and Doelling Boyd l and Utah, Ghost et al. - ( lived regressive D et al. ) , 2018;

Typical et al. , 1992; ing ( B ( , A )

)

This article isprotected rights by All copyright. reserved. middle Curtis. Major Transgression flooded the entire study area (and beyond), and marks the base of the three parasequenc experiencedsea allocyclicly the earthy facies transgressionsea Fig. probably underwent, similar cycles as itwas being depos suggest that the contemporaneous Summerville Formation could have undergone, and most that thefive, cyclical aeolian sequences identified in the Moab Member of the Curtis Formation the Curtis Formatio Fig. bundlestidal (TB) (Facies P). Organic Heterolithic sandstone with flaser bedding (Facies arrangedN), in rhythmic tidal bundle. Cross sandstone (Facies C), with rippled reactivation surfaces, bedding (FB) (Facies M, N), arranged in rhythmic tidal bundle. heterolithic deposits (FA 3). tidally (Facies R). (Facies L, M). (Facies R). Formation. See Facies Fig. waning bundles, migrating over subtidal, mud architectural arrangement of tha channel. Note its concave up, erosive base and flat upper surface (see Fig. 10for detail conglomerate, overlain by a gravelly dune. similar structure inthe gravelly dunes. the waxing Fig. Fig. 2 (Fertl prominentmore marine origin for these sediments, ratherthan a fully continental provenance t Fig. 5), and the upper Curtis palaeocurrent measurements for the lower Curtis (FA 2, FA 3, and FA 4), the corresponds to the Major Transgressive Surface (MTS). t Fig. Accepted Articlehorium/ correlativehe spatial distribution of facies associations across the Curtis basin. datum The Slick Slick Rock Member 9 8 7 6 5 4 - ...... for section location.

et al.,

stratified sandstone arranged in well - Duma Point sedimentary section and associated cyclical ( ( Summary basinal history for the Entrada E Common tide reworked flash flood deposits, migrating over a sole of mud A A - - rich (OM) toesets ofa cr W oriented correlation panel across the marine part and the aeolian Moab Member of ) ) u

Three differentThree conglomeratic deposits observable within the lower Curtis unit. Note N ranium (Th/U) genvalues - ( ( waning bundle arrangement ofthe upper gravelly channel and the absence of D B 1982). MorrisonThe Formation is shaded it as not ofis interest for this study. See - S of theEntrada Sandstone develo ) ) ( -

( C Heterolithic silt W oriented correlation panel along the NW margin ofthe San Rafael andSwell, Tangential cross F ) -

Bi G

had had started but hadnot yet es in thees lower Curtis, each ) - n. The datum corresponds to the Major Transgressive Su

- directional rippled cross As theAs Curtis startedsea regressing, the middle Curtis was coexisti dominated and tidally Table 1 forcodes

of theEntrada Sandstone - Summerville Formation intervals (FA 6 and FA 8).

- driven relative sea (

E stone ) -

Heterolithic silt stratified gravelly sandstone (Facies H), thought to result from oss t subtidal channel).

- and s stratified sandstone arranged in well erally belowfall 7 at approximately 5, which suggest a ( . B ( A - andstone lenticularwith (LB) and wavy bedding (WB) C ) ( - - )

modulated bedforms present in the Curtis D defined rhythmic tidalbundles (Facies P). Bi

- Clos

) stratified sandstone with episodic climbing ripples ped contemporaneously flooded - bounded by traceable

- dominated heterolithic flat deposits (FA 3a). lateral migration of asinuous subtidal, gravelly - directional rippled cross - stone level variations, leading to the development of Curtis . ( e - B up ofthebasal flash flood pebbly - ( D

E the study area and sandstone with wavy and flaser ) - )

Summerville interval

( As theAs Curtis kept sea transgressing, the Gravelly dune, arranged in waxing mud drapesmud and rip B ited. )

Rose diagrams displaying the

( g F amma )

Tangential cross -

to sand , the flooding surfaces. - to ray log. The - stratified sandstone

paralic deposits ofthe the - defined rhythmic

- dominated

rface (MTS). Note - : middle Curtis (FA aeolian dunes of up mud clasts. (A)

As theAs - stratified ( ( ng with H E

Curtis ) ) (

The The I - )

( ) .

This article isprotected rights by All copyright. reserved. Geosystems Inc. Acceptedcoarser Curtis, with thereplacement ofthe mud coarsening trend the from parts distal of thebasin and towards the shorel two other phases of tidal resonance before reaching maximal its extent Sztanó system entered in tidal resonance once thebasin threshold dimension reached.was After correlative energy level’s spatial distribution within the system Curtis Fig. 12 quasi exclusively a responseas of autocyclic forcing. contrasts with the amalgamation also testifies ofa potential impact of external forcing over the system. This intrinsically dynamic behaviour of thetide WSE parasequences. accompa one preceded the Major Transgression. Further, Parasequence 1 deposits, a second indicates that a first tilting oft developing.was illustrates the impact of both allocyclic and autocyclic forcing on the system as the lower Curtis overlyingstrata the J Entrada Sandstone, theerosive relief developed at its top, as well as the lower and middle Curtis Fig. 11 Transgressive System Tract; Flooding Surface;Article MTS = Major Transgressive Surface; MFS = Maximum Flooding Surface; TS Fig.See relationship variations contemporaneo itenteredonce in resonance, accompanied by the deposition of the middle Curtis, whereas the dot on the map), illustrating on the map), Gulch, leftred dot on the map) Fig. 10 deposits ofth and the coastal dune field terminated,was as the entire study area was occupied by the paralic the survival ofthe aeolian ofthe dunes Moab Member ofthe Curtis Formation wasshut down, sedimentary record. of autocyclic processes, and the marine part of the system wasunder the influence resonance, oftidal leading to the coastal dunes was dictated by allocyclically ofdunes theMoab Member ofthe Curtis Formation. development The ofthe paralic domain and the shallower upper Curtis, the depositssabkha ofthe Summerville Formation, and the aeolian - ENE laterally migrating subtidal channel (pink - like like basin during the lo . . . and de Boer ( -

11 ( Comparison between the relative sea Models representingModels the spatial distribution ofthe different FA across and idealised grained and cleaner sediments. nied by the shift of theFAs belt, resulted in the development of thethree A . The paralic succession also show ) for illustration phases.of uplift

Photogrammetric model ofCedar Mountain showing the earthy facies ofthe

between these observed cycles and the aeolian Moab Member e Summerville Formation. us Autocyclic forcing

Allocyclic forcing

middle Curtis’ system and its behaviour, which was impacted and developed aeolian 1995 ( - 3 Unconformity. H )

The Curtis sea )

deposits keptdeposits recording such allocyclicly ,

the transgressing Curtis is sea suggested to haveentered at least

the overwriting ofallocyclic signals by the tide HST wer Curtis, as well as the middle he Entradahe Sandstone strata occurred prior to thedeposition of , the paralic neighbouring systems at Duma Point (middle red dot overprinting ofthe

= High Stand : The angular: The relationship between the different strata :

one occurred before Parasequence 3 developed, and the last The minor spatio ( B kept regressing, and the sediment supply necessary to

- Pal

dominated FA 3a bydeposits, FA 3b’s and FA 4a’s - C

- RSME = Regressive Surface of Marine Erosion; FS = ) a - dominated system, but its multi

driven relative s of the Curtis Formation (Big Pinto Mesa, right red s with Vertically exagg eogeographic Map

- obvious cyclical floodings, but the level signal recorded by the marine part (Sven’s Syst

the effect of relative sea the

em em relative relative sea -

-

purplish tones) illustrate best th neighbouring system temporal energy variations, as well as the Tract

. erated interpreted model, which ea

- -

- upper Curtis intervals, and their ©2014 Colorado Plateau , both before and after the level variations level signature in the - forced relative sea

of ca. 800 km - level variations, ine in the lower s - -

remains puzzling story incision dominated system .

T accurate he shallowhe dominance . theNote e - level - - T = T . This article isprotected rights by All copyright. reserved. Accepted ArticleFacies D G A B C E F

stratified sandstone stratified Planar conglomerate Matrix sandstone condensed bioturbated Thoroughly sandstone fluidised Structureless sandstone cross Tangential evaporites localised with mudstone mottled parallel Plane Cross Description - stratified sandstone stratified - -

supported basal basal supported to low angle cross low angle to

TABLE TABLE 1 -

laminated to to laminated - stratified stratified

-

FACIES DESCRIPTIONTHE FOR ENTRADA SANDSTONE, CURTIS FORMATION AND SUMMERVILLEFORMATION -

lamination, unidirectional current unidirectional lamination, cross herringbone potential sandstone, white green to Plane cm. 20 thickness bed 8 cm, maximum Ø clast maximum sandstone, c matrix plane, bedding the to parallel be to axis tend long their but orientation preferred clast no well to Rounded cm. 25 maximumthickness bioturbated., thoroughly Rusty m. 2 thickness bed maximum 25 cm, Ø maximumboulder mudstone, injected with boulders visually visible, sometimes fluid local sandstone, grained silt pink to green of fluidised structureless Deformed to dm between ranging Thickness evaporite and/or cracks desiccation clasts, eventual rip and drapes mud potential surfaces, reactivation cross Trough cm. thickness 1 horizon maximumindividual horizons, rich evaporite localized rhizoliths, around patches bleached potential parallel plane lenses, sand vf white yellow to pale with mudstone silty red Dark foresets. of the counter of occurrence m.Potential thickness 15 dune individual maximum size, sets bedform/bedform varying rhizoliths, of occurrence local bleached, locally white, red or fall grain flow and grain alternating cross tangential Unidirectional Structures

- - parallel fine cemented, red condensed,

- stratified vf stratified -

to low angle low angle to

- rounded, matrix rounded,

- m - expressed as well rounded sandstone sandstone well rounded as expressed laminated to to laminated cross grained sandstone, common rippled rippled common sandstone, grained

- escape and loading structures still structures loading escape and - - bedded vf bedded

to m values. m to - - - stratified vf stratified supported basal conglomerate, conglomerate, basal supported , and oscillation ripple oscillation and , deposits, sharp base, rusty rusty base, sharp deposits, - onsists of f of onsists grained sandstone, sandstone, grained - stratified or mottled, mottled, or stratified - f grained sandstone, sandstone, f grained

- f grained gray to to gray f grained - ripples at the toe toe the at ripples -

to m - - up mud mud up - rich horizons. horizons. rich

f grained f grained - - - grained grained

- to fine to

- - VF Grain VF VF Si F size Si - F - Pb - -

- -

F Cl

M F F

with tidal influence. tidal with deposits beach to shoreface Upper deposits. Flash flood setting. plane coastal a in starvation Sediment horizons. saturated wate of liquefaction through or bed sandstone the through flowing fluids to structures due sedimentary original of Destruction dunes. Tidally vegetation. superficial and/or sabkha of development with domain plain coastal to interdune Aeolian level. table/saturated water migrating and dynamic a by influenced locally deposits, dune Aeolian Interpretation -

influenced migrating 3D migrating influenced occasional flooding with with flooding occasional

- type deposits type semi r - -

arid arid -

Curtis Fm. ? Curtis Fm. Ss Entrada Curtis Fm. Ss Entrada Fm. Summerville Curtis Fm. Fm. Entrada Fm. Summerville Ss Entrada Mbr. Moab Ss Entrada Formation

AcceptedThis article isprotected rights by All copyright. reserved. Article M N H K L J I

Heterolithic sandstone with with sandstone Heterolithic bedding wavy with sandstone silt Heterolithic bedding lenticular with sandstone silt Heterolithic mud parallel Plane conglomerate sandy stratified sigmoidal to Planar sandstone conglomeratic stratified Tidally sandstone gravelly cross Tangential -

to siltstone to - influenced cross influenced

-

laminated laminated - -

- and and and stratified stratified

cross - - sandstone, scattered mud lenses, as well as single and double double single and as aswell lenses, mud scattered sandstone, herringbone and Ripple v planes, bedding the to normal parallel and both bioturbations sporadic cracks, desiccation occasional green siltstone, to gray laminated with interbedded and indicators current directional cross Ripple planes. bedding the to normal and parallel both bioturbations sporadic cracks, desiccation green mud to gray laminated matrix of cross ripple current and herringbone vf Rippled planes. bedding the to normal and parallel both bioturbations sporadic cracks, desiccation cross ripple current parallel Plane thickne individual maximum cross planar 2.5 cm, Ø clast maximum clasts, convex Clast cm. thickness 60 bed cross sub rip bundles, tidal in amalgamated and developed locally extent, lateral restricted of conglomerate Matrix m. thickness 2.50 cross trough current unidirectional cm, Ø 2.5 clast clasts, maximum rounded to sub Matrix 60 cm. thickness bed individual maximum as dm aswell lamination, arying amount of organic matter. of organic amount arying - - horizontal erosive base, rip erosive base, horizontal

- cm, bidirectional Ø 2.5 clast clasts, maximum rounded to -

stratification with superimposed current superimposed with stratification to matrix to - - - hm dune, conglomeratic supported down erosive base, flat top, extra top, flat base, erosive down to clast to - f grained sandstone, grayish lenses containing lensescontaining grayish sandstone, f grained - stratified vf stratified - laminated mud laminated - - supported lense supported supported conglomerate, hm conglomerate, supported

- stratifications gray to green, occasional green,occasional to gray stratifications -

stratification, maximum individual dune dune maximumindividual stratification,

cross - f grained grayish sand layers, with bi with layers, sand grayish f grained - scale soft sediment deformation, deformation, sediment softscale ss 3.00 m. 3.00 ss - - stratified vf stratified

to - - up mud mud up shaped intraformational intraformational shaped siltstone, scattered bidirectional bidirectional siltstone, scattered - up mud clasts, mud up

- stratifications within a a within stratifications

-

to clasts, extra - -

basinal sub basinal f gray to green to white white to green to f gray - siltstones, occasional occasional siltstones, scale lateral extent, extent, lateral scale - stratification, stratification, - scale lateral extent, extent, scale lateral - ripples, maximum maximum ripples, extra - basinal sub basinal -

- to rounded rounded to basinal basinal - - -

M M VF Si F Si Si - - - -

- -

Gr -

Gr Gr Cl

F F F

Upper sub Upper L). Facies than (shallower zone subtidal reversals in Current zone. subtidal lower reversals in Current reversa related current tidally with flow activity Gentle channel. tidal migrating a within accretion lateral bar Point channels energy tidal High embayment. restricted laterally a within pattern flow tidal asymmetric energy, High

-

to lower intertidal intertidal lower to

ls.

- inlets. -

Curtis Fm. Mbr. Moab Curtis Fm. Curtis Fm. Curtis Fm. Curtis Fm. Curtis Fm. Curtis Fm.

AcceptedThis article isprotected rights by All copyright. reserved. Article Q O U V R P T S

Plane parallel Plane sandstone cross Rippled sandstone Condensed sandstone parallel Plane sandstone cross rippled bi Thoroughly sandstone Structureless bundles tidal rhythmic well in arranged Cross ripple climbing with Sandstone bedding flaser - s stratified sandstone sandstone stratified

- - - - stratified - stratified stratified

laminated laminated stratified stratified directional directional - defined defined

Dark red soft slope forming siltstone, most probably plane plane probably most siltstone, forming slope soft red Dark deformations. sediment soft cracksand mud potential current 3D with sandstone, cross rippled to Undulated cm. C of the Tongue Member Moab the capping exclusivelyobserved undulations, amplitude low displaying occasionally sandstone, yellowstructureless Thin, deformations. sediment soft cracksand mud Potential CurtisFm. the of units different the variesbetween facies this of expression weathering pink white, lamination, ripple current parallel Plane cross herringbone silt rippled Thoroughly weathered. smoothly and rounded single and scattered potential Vf matter. of organic amount varying toesets, anti occasional with bundles, tidal Vf green. cross Climbing ripple matter. of organic amount varying drapes, mud - - f grained gray to green to white sandstone, massive, with with massive, white sandstone, green to to gray f grained f(

- m) grained gray to green to white sandstone, arranged in in arranged sandstone, white to green to gray m) grained

-

stratified vf stratified - stratifications, potential climbing ripples. climbing potential stratifications, - stratified vf stratified -

to vf to urtis Fm. Maximum bed thickness 10 thickness bed Fm.Maximum urtis - f - - stratified vf stratified ripples, possible interference ripples, ripples, interference ripples, possible grained sandstone with scattered scattered with sandstone grained - grained sandstone, dominated by by dominated sandstone, grained - or double mud drapes. Usually Usually drapes. mud double or - f grained sandstone, gray to to gray sandstone, f grained - ripples documented from their their from ripples documented

or green. Note that the that green. Note or - f - grained, gray to brown to gray grained,

- VF (VF (S VF S VF VF M) - - - Si - F

- ) VF

F VF - - - F

F (

F F F -

) - Supratidal plain. Supratidal conditions. current unidirectional under ripples 3D migrating horizon. Condensed short Documented lowerantidune (to flow regime upper sandflat, Tidal structures. sedimentary some in ca can weathering the that Note conditions. current tidal ebb and flood equal near with environment Deep subtidal environment. sub indicate drapes of mud Presence weathering. surface intensive to due be might only structure of lack the of The nature I. Facies energy than inlets,Tidal lower sandflat. sub Upper flat, tidal spill on overbank channel Tidal sandflat.

- lived subaerial exposure. subaerial lived

mud cracks indicate cracksindicate mud

ses erase most of the of the most ses erase - -

regime?). regime?). to lower intertidal intertidal lower to

-

or intertidal intertidal or

Summerville Fm. Summerville Mbr. Moab Curtis Fm. Ss Entrada Mbr. Moab Mbr. Moab Curtis Fm. Mbr. Moab Curtis Fm. Curtis Fm. Curtis Fm. Curtis Fm.

AcceptedThis article isprotected rights by All copyright. reserved. Article W X

Palaeosol sandstone laminated ripple rich Iron siltstone

-

and parallel and

- Dark purple mud or silt. or mud purple Dark cross vf cemented brown to red Dark evaporites. parallel - stratifications, potential desiccation cracks. desiccation potential stratifications, - laminated, scattered pale white bleached lenses and lensesand bleached white pale scattered laminated,

- f - grained sandstone, gentle ripple ripple gentle sandstone, grained

VF M - - S

F

superficial soil development. superficial sub deposits. Fluvialoverbank - aerially exposed surface exposed aerially

with with Fm. Summerville Mbr. Moab Curtis Fm. Ss, Entrada Fm. Summerville Fm.

This article isprotected rights by All copyright. reserved. FA 8 FA 7 FA 6 FA 5 FA 4b FA 4a FA 3b FA 3a FA 2 FA 1b FA 1a Association Facies Accepted Article TABLE 2

-

FACIES ASSOCIATIONS FORTHE ENTRADA SANDSTONE, CURTIS FORMATION AND SUMMERVILLE

Coastalaeolian dry dunefield (Mountney, a more stressed environmentthan FA 3. subaerial exposures and rarebioturbation, indicator of complex, upward finning, with intermittentprolonged Upperintertidal heterolithic tidal dunesand tidal bars. environments, encompassing tidal flats, tidal channels, High energy,sub in4a the northern areas. Tidal channel infills and splays, distal correlative of FA with potential subaerial exposures. Sandy tidal flat with correlative major tidal channels, bedded sandstone,scarsely bioturbated. generally upward coarsening from wavy Subtidal heterolithic vf bioturbated. mudstoneto wavy beddied sandstone, scarsely generally upward coarsening from laminated Subtidal heterolithic mud potential associated tidal channels cut Beach deposits to uppershoreface deposits, with soil interdunesdeposits and superficial development of 2012), with episodic (marine) partial flooding of system(Kocurek and Havholm, 1993; Mountney, Coastal wetaeolian interduneand lower coastal plain horizons. superficial development of soil (marine) partial flooding of interdunesdeposits and Havholm, 1993; Mountney, 2012),with episodic Coastal wetaeolian dune system (Kocurek and Environment Depositional flooding. Supratidal lowercoastal plain, sedimentsand/or palaeosol canbe observed. supersurfaces, upon which transgressive water arranged in five sequences separated by -

and vegetated horizons.

-

to intertidalto -

to

-

, f silt - grained sandstone channels and flats

- sand with episodic marine -

vf and vegetated FORMATION - grained sandstone,

- dominated - and -

to flaser

2012), - fill.

- carried

H, I,J,K, L, M S, C, G, U B, C, X D, A, C,X Facies Included U, V,W, X X A, N, S, Q, U, T, U, X L,K, M, N,Q, S, X) N, O, Q,P, S(, R, (K,C, G, L, M,) S, U C, H,I, L, N, M, S, U,X H, I,M, N

Curtis Fm. Curtis Fm. faciesearthy Sandstone Entrada Slick Rock Mbr. Sandstone Entrada Formation SummervilleFm. Moab Mbr. Curtis Fm. Curtis Fm. Curtis Fm. Curtis Fm. Curtis F Curtis Fm. m.

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article

This article isprotected rights by All copyright. reserved. Accepted Article