Dynamic Carboniferous climate change, Arrow Canyon, Nevada

James W. Bishop* Isabel P. Montañez David A. Osleger Geology Department, University of California–Davis, Shields Avenue, Davis, California 95616, USA

ABSTRACT driven by a single, large ice sheet. Rather, Isbell et al., 2003a, 2003b, 2008a, 2008b; Field- the Arrow Canyon archive of varying depo- ing et al., 2008a, 2008b, 2008c, and references The Phanerozoic’s longest-lived and most sitional facies and cycle stacking patterns therein). These records argue for intervals of widespread glaciation, the late Paleozoic ice records major changes in the magnitude of glacial minima during the late Paleozoic ice age, age, is undergoing a resurgence in interest. short-term glacioeustasy. This fi nding con- with geographically restricted ice centers or pos- Long-held models of the timing, duration, tributes to recent and growing near- and far- sibly ice-free conditions near the South Pole for and magnitude of glaciation are being reeval- fi eld evidence for a more dynamic glaciation periods of several million years. This conclusion uated due to emerging evidence from former history than previously inferred from the calls into question how fl uctuating continental high latitudes, evidence that the late Paleo- classic Euramerican cyclothems. ice sheets could have sustained large (>50 m) zoic ice age was punctuated by long-lived gla- sea-level changes throughout the late Paleo- cial minima or possibly ice-free times. INTRODUCTION zoic. Moreover, recent studies of some far-fi eld The history of the late Paleozoic ice age cyclothem records also suggest varying charac- is archived within the biostratigraphically Much of our understanding of the late Paleo- teristics of cyclothems, with intervals of poten- well-constrained, carbonate-dominated suc- zoic ice age (LPIA) has been built on stratigraphic tial lower amplitude glacioeustatic forcing (e.g., cession of Arrow Canyon, Nevada, United records from the low-latitude tropics, typifi ed by West et al., 1997; Smith and Read, 2000; Wright States. In this paleo-tropical succession, Euramerican cyclothems. These far-fi eld records and Vanstone, 2001; Gibling and Giles, 2005; the distribution of lithofacies, fl ooding sur- preserve high-frequency sequences of open- Heckel, 2008). Accordingly, climate simulations faces, and subaerial exposure horizons and marine, paralic, and terrestrial environments. indicate that the response of ice sheets to orbital

their stacking into meter-scale cycles record Cyclothems have long been considered the most forcing was quite sensitive to variations in pCO2 a detailed climate history. The onset of this sensitive proxy of high-frequency (105 yr) gla- and overall ice sheet size, leading to a range phase of glaciation during the middle Mis- cioeustasy, driven by the waxing and waning of of possible glacioeustatic magnitudes (Horton sissippian was followed by a dynamic evolu- expansive ice sheets in Southern Hemisphere et al., 2007). Thus, changes in the frequency tion of glacioeustasy through the late Missis- Gondwana (e.g., Wanless and Weller, 1932; and amplitude of Carboniferous–Permian gla- sippian to late Pennsylvanian. Moderate- to Wanless and Shepard, 1936; Heckel, 1977). cioeustasy should be expected during the course high-amplitude glacioeustasy was likely The persistence of cyclothems in upper Missis- of the late Paleozoic ice age if the extent and vol- interrupted by an earliest Pennsylvanian sippian through lower Permian successions has ume of stable continental ice sheets varied. This short-lived glacial minimum, but otherwise been argued as evidence for repeated short-term hypothesis, however, has been minimally tested appears to have persisted through the mid- (20–400 k.y.), high- amplitude (30 to >150 m) in the low-latitude paleo-tropical basins. dle Pennsylvanian. sea-level changes, and in turn the persistence of This study documents lithologic, pedogenic, Upper Pennsylvanian strata record low- large-scale continental glaciation throughout an and early diagenetic facies and their stratigraphic to moderate-amplitude relative sea-level ~50 m.y period of the Carboniferous–Permian stacking into meter-scale cycles in the Carbon- changes, suggesting a long-lived interval of (Heckel, 1977, 1986, 1994, 2002; Veevers and iferous succession of Arrow Canyon, Nevada, diminished ice volume. This proposed glacial Powell, 1987; Horbury, 1989; Frakes et al., United States. This carbonate- dominated suc- minimum is coincident with a notable mini- 1992; Soreghan and Giles, 1999a; Smith and cession has nearly complete exposure, relatively mum in glaciogenic sedimentation near the Read, 2000; Cook et al., 2002; Zempolich et al., high subsidence rates, and a very well con- former southern pole, aridifi cation across 2002; Heckel et al., 2007). strained biostratigraphy; in addition, carbonates paleo-tropical Pangea, and signifi cant fl o- This paradigm has been challenged by emerg- tend to fi ll accommodation space and are thus ral and faunal turnover, suggesting a link ing near-fi eld records. In particular, recent com- highly sensitive to climate change and siliciclas- between tropical environmental change and pilations of paleo–high-latitude Gondwanan tic input. Our approach is to use the changes in high-latitude glaciation. These conclusions, records document discreet intervals of wide- facies and cycle types to reconstruct ~30 m.y. however, are at odds with those tradition- spread glaciogenic sedimentation, punctuated of Carboniferous relative sea-level and climate ally inferred from Euramerican cyclothems, by periods of normal marine or fl uviodeltaic history on the paleo-tropical western margin of i.e., persistent high-amplitude glacioeustasy sedimentation, or long-lived pedogenesis (e.g., Euramerica. Though we show that the long-term

*Present address: Chevron Energy Technology Company, 6001 Bollinger Canyon Road, C-1217, San Ramon, California 94583, USA; [email protected].

Geosphere; February 2010; v. 6; no. 1; p. 1–34; doi: 10.1130/GES00192.1; 17 fi gures; 4 tables.

For permission to copy, contact [email protected] 1 © 2010 Geological Society of America

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accommodation record is dominated by subsid- effects of the Ouachita-Marathon orogeny and a nearly complete Famennian to Wolfcampian ence variations, the short-term high-amplitude thus be linked to the Ancestral Rocky Mountains carbonate-dominated succession. relative sea-level record is inferred to refl ect (Kluth and Coney, 1981; Kluth, 1986; Dickin- the repeated waxing and waning of Gondwa- son, 2006). Alternatively, they may relate to a METHODOLOGY AND nan ice sheets. A tectonic explanation for such continuing post-Antler tectonic evolution of the CHRONOSTRATIGRAPHY moderate- to high-amplitude relative sea-level western margin of North America (Trexler et al., changes is ruled out by their character, longev- 1991, 2003, 2004; Stevens and Stone, 2007). A composite section was measured on both ity, bounding surfaces, and the record of coeval Platform geometries evolved during the sides of Arrow Canyon, encompassing Osagean glaciogenic sediments in high latitudes. Thus, course of Carboniferous sedimentation. We through lower Virgilian (Visean through Gzhel- the presence and magnitude of such short-term use “platform” in the sense of Read (1985) to ian Russian Platform stages) strata of the Yel- changes are taken as proxy for minimum pos- encompass both ramps and shelves. Middle to lowpine, Battleship Wash, Indian Springs, and sible ice volume (cf. Read, 1995; Smith and late Mississippian Arrow Canyon strata accu- Bird Spring Formations. Upper Virgilian and Read, 2000; Wright and Vanstone, 2001). In mulated on a carbonate or mixed carbonate- Wolfcampian strata are heavily recrystallized, particular, in this paper we note the absence siliciclastic ramp, with correlative basinal facies obscuring many depositional and early dia- of such moderate- to high-amplitude relative to the west in western Nevada and Death Val- genetic features; these strata are not discussed sea-level changes during intervals traditionally ley (Stevens et al., 1991; Poole and Sandberg, here. Above the base of the Indian Springs For- ascribed to peak glacioeustasy (e.g., late Penn- 1991; Trexler et al., 1996). During Pennsylva- mation, the section was tied to a standard can- sylvanian), an absence that cannot be explained nian time, the study area was on the northeast yon section, measured by Amoco Oil Company by tectonic drivers. Because the lack of high- Bird Spring platform of the Keeler Basin (also as part of an extensive biostratigraphic research amplitude glacioeustasy might be due to small known as Bird Spring Basin; Kluth, 1986) that program in Arrow Canyon, and along which ice sheets or the presence of a very large, stable initiated as a ramp during the early Pennsyl- brass tags and metal spikes were affi xed every ice sheet (DeConto and Pollard, 2003; Horton et vanian (Morrowan; Stevens et al., 1991, 2001; 1.5 m (stratigraphic locations in this paper are al., 2007), we look to the high-latitude record of Stevens and Stone, 2007) but evolved into an labeled with an “A” prefi x, corresponding to this glaciogenic sedimentation to distinguish large, attached shelf by late Pennsylvanian time. Dur- standard measured section). To refi ne lithofacies stable ice sheets from small, feckless ones. ing Morrowan, Atokan, and possibly early Des- interpretations, identify faunal assemblages, and Different climate modes are suggested for moinesian time, the Bird Spring platform was a describe early diagenetic features, 663 samples the Arrow Canyon succession by changes in distally steepened ramp, indicated by rare sedi- were collected, thin-sectioned, stained with patterns of meter-scale cyclicity and facies dis- ment gravity fl ows in the basin (Yose and Heller, Alzarin red and potassium ferricyanide (Dick- tributions. These changes delineate intervals 1989; Miller and Heller; 1994), unrestricted son, 1965), and examined under transmitted and of distinct short-term relative sea-level fl uctua- storm-dominated strata in Arrow Canyon, and cathodoluminescent light. tions and regional climate. These intervals are the absence of evidence for any margin (e.g., Biostratigraphic control is provided by con- ultimately linked to changing glaciation by ties biohermal buildups or grainstone shoal com- odonts, calcareous algae, foraminifera, and between ice volume and eustasy (e.g., Read, plexes at a break in slope). By contrast, in upper fusulinids (Appendix A). The thick, relatively 1995; Smith and Read, 2000), and between con- Desmoinesian through Wolfcampian time, the complete Arrow Canyon succession includes tinental ice sheets and low-latitude precipitation Bird Spring platform prograded westward and the Global Stratotype Section and Point for (Cecil et al., 2003; Poulsen et al., 2007). The evolved into a (locally) rimmed shelf, as evi- the Mississippian-Pennsylvanian boundary Arrow Canyon succession records the onset of denced by abundant turbidites, debris fl ows, (Brenckle et al., 1997; Lane et al., 1999; Rich- glacioeustasy in basal Chesterian time, a short- and megabreccias in basinal settings (Yose and ards et al., 2002; Ellwood et al., 2007; Barnett lived glacial minimum in earliest Morrowan Heller, 1989; Miller and Heller; 1994), restricted and Wright, 2008; Bishop et al., 2009), and has time, and a long-lived, signifi cantly drier glacial platform interior facies in Arrow Canyon, and been a focus of biostratigraphic research for minimum during later Desmoinesian through phyloid algal bioherms with bypass channels, nearly 50 yr (Cassity and Langenheim, 1966; early Virgilian time. which mark the shelf margin in the Nevada Test Webster, 1969; Pierce and Langenheim, 1972; Site and Death Valley (Miller and Heller, 1994; Rice and Langenheim, 1974a, 1974b; Langen- TECTONIC AND GEOLOGIC SETTING Stevens et al., 2001). heim et al., 1984; Baesemann and Lane, 1985; Nearly continuous, high subsidence in Brenckle, 1997; Stamm and Wardlaw, 2003). The Arrow Canyon Range is in southeastern the Arrow Canyon region promoted a thick, Chronostratigraphy for this study is based pri- Nevada, in the eastern Great Basin province. relatively stratigraphically complete Carbon- marily on extensive Amoco biostratigraphic data, During the middle to late Paleozoic, Arrow iferous succession. Long-term (second- to collected over several decades, and subsequently Canyon was situated in the tropics on the west third-order) accommodation in this setting donated to the Universities of Iowa (conodonts) coast of the North American craton, near the sea- was driven by regional tectonics; however, and Kansas (foraminifera) (Groves and Miller, ward margin of an interior seaway that at times this study examines the high-frequency strati- 2000). This biostratigraphic control begins below extended from California to Alaska (Poole and graphic record to extract climatic signatures the Osagean Yellowpine Formation and contin- Sandberg, 1991; Ross, 1991) (Fig. 1). Southeast- during the Carboniferous interval. Most of the ues through the Chesterian to lower Wolfcam- ern Nevada was in the foreland basin inherited succeeding Permian and Mesozoic strata were pian Bird Spring Formation. Many of the range from the Devonian–early Mississippian Ant- removed by a regional unconformity caused charts and original thin sections have since been ler orogeny (Dickinson, 2006). During middle by the Cretaceous Sevier orogeny (Page and reinterpreted (Leavitt, 2002; Vladimir Davydov, Mississippian to early Permian time, the former Dixon, 1997). During Neogene time, basin and 2007, personal commun.; Greg Wahlman, 2006– foreland evolved as a series of basins and uplifts. range extension uplifted the Arrow Canyon 2007, personal communs.; Bishop et al., 2009) Tectonic controls on this structural landscape Range in a north-south–trending block, and and are used here. Appendix A presents the pre- are not well constrained and may relate to distal canyons cutting through the range now expose ferred biostratigraphic zonation tied to meterage,

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A numbers, and the bed numbers of Cassity and we divide into broad depositional settings: their Dunham textures, sedimentary structures, Langenheim (1966) where appropriate. outer, middle, and inner ramp (Mississippian and photozoan versus heterozoan grain types. to middle Pennsylvanian) and shelf interior Heterozoan fossil assemblages consist primar- LITHOFACIES AND DEPOSITIONAL (upper Pennsylvanian). Lithofacies descriptions ily of echinoderms, bryozoa, brachiopods, fora- ENVIRONMENTS for each are provided in Tables 1–4. In the fol- minifera, solitary corals, calcareous red algae, lowing we highlight salient features of each set- sponge spicules, and trilobites. Photozoan Carboniferous strata in the study area were ting and offer an environmental interpretation. assemblages consist primarily of coated grains, deposited on a westward-facing platform that Lithofacies are defi ned and interpreted using peloidal lime mud, fully micritized grains,

Stage Per- Faunal Formation meters iod global N.A. zone Per- Asse- Wolf- Schwag- 900 A mian lian campian erina (Bursumian) Virgilian

Triticites 800

700

Figure 1. (A) Middle Penn- Bird Spring sylvanian paleogeography (after Blakey, 2007). Circle Fusulina 600 indicates Arrow Canyon, within 10º of the equator. B Keeler (Bird Spring) Basin Inset shows Missourian during Late Pennsylvanian paleogeography of western Eroded Antler Belt Source North America. (B) Late Sea-level Fusu- 500 Pennsylvanian schematic linella of the Keeler–Bird Spring

Tippipah Profu- Basin, with Arrow Can- Platform Bird Spring Arrow sulinella yon positioned on the Bird Shelf Canyon Spring shelf (after Miller and Heller, 1994). (C) Topo- 400 graphic map showing the Supai (?) source location of sections mea- sured in Arrow Canyon (USGS, 1986). (D) Biostrati- Eoschubertella Pseudostaffella & Pseudostaffella graphic zonation for Arrow

Bashkirian Moscovian300 Canyon, Kasimoviancompiled Gzelian from Bird Spring Appendix A.

C sym- metricus sin- min

Morrowan Atokan200 Desmoinesian Missourian D. nodul. 14 13 Indian 12 Springs

Chesterian 100 Serpukhovian 9 & 10 Battleship 8 Wash Mississippian Pennsylvanian Mera- mecian 500 m 7 Yellowpine Visean

N Osag- ean 0

Geosphere, Februrary 2010 3

Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/6/1/1/3337767/1.pdf by guest on 24 September 2021 Bishop et al. (b) (b) >50 (c)>50 Water Water depth (c) >40 (c) >40 40–70 20–60 20–60 c)(b, (b, d) d) (b, 35–40 35–40 15–40 15–40 15–30 15–30 depth (m) Water Water environment environment SWB SWB, dysoxic pore pore SWB, dysoxic waters environment environment upwelling waters SWB pro- SWB, locally to shoreface likelyby bathed delta or lower delta offshore Depositional and SWB and/or coated from shoals, grain banks and FWWBSWB to Deep subtidal,below Depositional Depositional Between FWWBBetween

c i t nd (c) below SWB. o i b common euhedral carbonate- pyrite and cemented nodules Silt-sized peloids; Silt-sized peloids Proximal or below to Silt-sized peloids SWB, below Near to A

c i t o i b pseudomorphs after ikaite Silt-sized peloids above Near to A Rare glendonite Coated grains, locally peloidal locally peloidal grains, Coated skeletal of Seaward Components Component

c i t o i locally common whole brachiopod locallybrachiopod common whole echinoderm columnals,solitaryand common calcite-filled after molds articulated bryozoa, brachiopods, valves and shells, articulated corals spicules; locallyspicules; commonthin-walled common calcite-filled after molds bryozoa, articulated crinoid columnals, echinoderm columnals, solitary corals echinoderm spicules, thin-walledbrachiopods, solitary corals

c Mostly unidentifiable silt-sized bioclasts; Mostly unidentifiable B Unidentifiable silt-sized bioclasts; Unidentifiable Unidentifiable silt-sized bioclasts; Unidentifiable i t o i sponge spicules common calcite-filled after molds trilobites, solitary corals,forams, spicule molds, brachiopods (spines), brachiopods molds, spicule rare redalgaeand mollusks articulated echinoderms, rare sponge solitary corals trilobitesand spicules shells, forams, bryozoa, fusulinids, B Common echinoderms, bryozoa, bryozoa, Common echinoderms, Common whole brachiopod valves and valves and Common brachiopod whole TABLE 2. MID-RAMP FACIES TABLE 1. OUTER-RAMP 1. FACIES TABLE locally partially to packstone, dolomitized packstone Calcisiltite silt-sized bioclasts; Unidentifiable mudstone to dolomitized dolomitized wackestone, locally with little texture, with little texture, spiculitic calcisilt, dolomitized locally Wackestone to Lime wackestone Argillaceous, silty lime lime silty Argillaceous, Lithology Calcisilt, locally Recrystallized chert chert Recrystallized Quartz silt, mica, clay Rarebrachiopod, crinoidossicle N/A Below FWWB and and centimeter centimeter insoluble- thin by lamination defined defined lamination seams rich bioturbation structures lamination, minor minor lamination, lamination, minor minor lamination, Nodular to wavy lamination, lightly bioturbation. chertbedded inuous millimeter millimeter inuous burrowed Millimeter Millimeter Millimeter to to Millimeter Local millimeterLocal Even to discont- bioturbated; locally mm- muddy grainyscale and muddy laminations laminations muddy laminations laminations current and/or wave- ripples Sedimentary structures Sedimentary Lithology Low-angle truncation, rare Typically thoroughly Well-burrowed grainy grainy Well-burrowed gray, black to black gray, to surface nodular; chalky, purple on fresh with black chert decimeter scale; scale; decimeter gray limestone blue-gray blue-gray blue-gray brown, surface wavy beds; blue- to black on fresh scale; gray gray scale; color to meter to tan to decimeter to meter gray scale; to blue- scale; decimeter decimeter gray Decimeter-scale Decimeter-scale Massive to Red to yellow to to yellow to Red Decimeter Decimeter Centimeter Centimeter Centimeter Centimeter : SWB—storm: wavebase; FWWB—fair weather wavebase; W/P—wacke-packstone. (b) Between FWWBSWB; and (d) withinphotic zone. : Outer-ramp: facies. Parenthetical lettersafter waterdepth rangecorrespond with (b) between FWWB and storm waveSWB,base, a (MR7) (MR7) heterozoan (MR6) W/P W/P W/P W/P photozoan (MR5) (MR5) calcisiltite calcisiltite and siltstone and (OR4) interbedded (OR2)chert mudstone mudstone laminated calcisiltite (OR3) Note Offshore Offshore Note Offshore Offshore

Facies Bedding and Facies Bedding Cross-stratified Marl (OR1) to Massive Wavy Massive to Laminated Facies Bedding and color Sedimentary color and Facies Bedding

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) l (

(a) e, g) e) g, h, i) e) e) e, g) (m) (m) 2-5 (a, (a, 2-5 2-20 (a, 0 0-2 (k) 0-2 depth <1-15 5-20 (a, 1-5 (j)1-5 0-5 (a,d, 5-20 (a, 1-20 (a) 0 (l)

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r l i o a evaporative lagoon flats) flats) between shoals and tidal cryptmicrobial laminites h o FWWB, may bioherms baffle mud to above FWWB above FWWB swept by currents shoals and shorelines, near to above FWWB shoreface shoreface transgressions transgressions S M Shallow subtidal,above Shallow subtidal,photic, Shallow, highly highly restricted, Shallow, Shoals and shorelines near Shallow, wave-washed wave-washed Shallow, Evaporative lagoon 2-20 (a, Intertidal to supratidal; Depositional environment Water S

n o m m o c

g n i n i

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i a t e d Evansd (1973), (f)al.(1970),et Logan (g) Logan Hagan and o m n i micritized grains sized peloids; local peloids; sized grains, peloids peloids grains, coatings, micritizedcoatings, sand- cauliflower chert grains, fully micritized micritized fully grains, anhydrite pseudomorphs local cauliflower chert e o cauliflower chert common cauliflower chert anhydrite pseudomorphs after anhydrite pseudomorphs after micrite envelopes oncolitic coatings, rare coatings, oncolitic oolitic coatings,thick b H Peloids, coated grains; Clotted micrite, coated Peloids, coated grains, fully Abundant peloids;Abundant common Common oncolitic oolitic, Oncolitic to oolitic cortices;oolitic Oncolitic to Peloidal matrix, common Peloidal Common silt-sized peloids Lagoonal (positioned N A Component coral heads, )colonial and ) corals, ) corals, Syringapora Siphonodendron, Syringapora

c e i t n trilobites, Chaetetes, matrix similar toIR10, or MR7) IR12, rugose ( rugose encrusting) common mollusks, mollusks, common encrusting) Cystolonsdaleia brachiopods, bryozoa, solitary corals, echinoderms, forams, fragments, brachiopods, bryozoa, echinoderms, forams, trilobites solitary corals, forams, rare rare forams, solitary corals, (spines),trilobites, spicules, mollusks and coralline red algae o o bryozoa, fusulinids fusulinids bryozoa, brachiopods (spines),bryozoa, crinoids heads and shells, articulated crinoid fronds, muddy matrix and shells, forams, fusulinids, solitary coralsbryozoa, trilobites and articulated echinoderms; mollusk molds; rarechaetetes, sponges and Syringapora coral stems, solitary corals;bryozoa i facies; rhizolithsand redoximorphic roothaloes Abundant foramsAbundant (commonly Tabulate ( Mostly as nuclei: fusulinids, coral fusulinids, Mostlynuclei: as Fusulinids, Fusulinids, B Echinoderms, bryozoa, brachiopods N Brachiopods (spines), trilobites; rare Common whole brachiopod valves Common brachiopod whole Common large fusulinids, fusulinids, Common large Common whole brachiopod valves TABLE 3. INNER-RAMP FACIES grainstone chert nodules dolomitized packstone sized quartz packstone packstone, variably wackestone, and packstone cherty packstone, variable dolomite packstone, variable dolomite, chert nodules Argilisols, and and Argilisols, Vertisols Dolomudstone, Dolomudstone, Local cauliflower Local Boundstone and Grainstone to Dolowackestone and Framestone, variably Wackestone and Silt to medium sand Lime grainstone to Quartz siltsand and Rarely, rhizoliths Quartz silt to very fine sand Eolian, reworked during sand in troughs diameter, <30 cm high, unknown unknown cm high, <30 diameter, common, rare wave ripples ripples wave rare common, synoptic relief;quartz and lime bioherms and biostromes stratified stratified stratified, rare currentand/or wave ripples ripples wave stratification stratification tabular and rarelytrough cross- mudcracks, crinkly with LLH LLH with crinkly mudcracks, laminations of mud and local grainytraction deposits structures structures peloids/skeletal grains, fenestrae, stromatolites,filland cut local grainytraction deposits centimeter “pinstripe”cross-centimeter lamination lamination cracks, soil pisoids;structure,ped horizonation, slickensides Planar tabular cross-stratification Micriticcm 1-5 thrombolite, Planar tabular to trough cross- Typically thoroughlybioturbated, centimeter to millimeter Planar Thoroughly bioturbated Wackestone to Sedimentary structures Sedimentary Lithology Typically thoroughlybioturbated, Typically bioturbated, localplanar- Planar tabular to trough cross- Massive, rarely even millimeter to to millimeter even rarely Massive, wacke-packstone; FWWB—fair weather wave (a)base. Above FWWB, (d) withinphotic zone, (e) Purser an scale beds; blue blue meter scale; meter scale; tan meter scale; blue-gray to to blue-gray blue, gray, tan color red to yellow to meter scale; meter scale; gray blue, gray meter scale; Decimeter to Decimeter Decimeter decimeter locally blue locally blue massive; tan massive; tan Massive; tan Massive; tan diameter Decimeter meter to meter scale; meter scale; gray or meter scale to tan Centimeter to Centimeter to meter scale or meter scale scale; tan, Centimeter to to Centimeter massive; gray Decimeter to scale; yellow-scale; decimeter meter scale; meter scale; brown red red yellow-red- Centimeter to to Centimeter Decimeter to to Decimeter Decimeter to to Decimeter Centimeter to to Centimeter : G/P—pack-grainstone; W/P— (IR10d) (IR10d) (IR10b) (IR10b) (IR10c) (IR10) (IR10) framestone sandstone (IR8) (IR9) Thrombolite Thrombolite Metazoan Coated G/P G/P Coated W/P (IR12) (IR12) W/P photozoan W/P (IR12b) Photozoan G/P Cross-stratified W/P (IR11) (IR11) W/P Facies Bedding and Facies Bedding Heterozoan G/P sandstone (IR15) Note Dolomitized Dolomitized Laminite (IR13) Laminite to Centimeter Lagoonal heterozoanLagoonal Lagoonal photozoanLagoonal Paleosol (IR14) Centimeter to Roots, glaebules, circum-granular Calcisols, Protosols, Those of overprinted limestone Soil pisoi Calcareous Calcareous

(1974), (h)LoreauPurser and (1973), (i) Harris (1979), (j) Oslegerand Read (1991), (k) intertidal,and (l) supratidal.

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Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/6/1/1/3337767/1.pdf by guest on 24 September 2021 Bishop et al. (m) (m) depth e) d, g, h, i) e) (a) e, g) e) Water Water 0 (l) 0–2 (k) 0–5 (a, 2–5 (a, 0–5 (a, <1–15 1–5 (j) 5–20 (a, environment Depositional transgressions transgressions during during lagoon crypt-microbial crypt-microbial laminites restricted, restricted, evaporative lagoon bioherms maybaffle washed shoals and FWWB above FWWB, mud shorelines, above photic, sweptby currents near to above FWWB Evaporative lagoon 2–20 (a, Highly restricted Shallow estuarine estuarine Shallow 2–20 Intertidal to supratidal; Shallow, wave- Shallow, Shallow subtidal, subtidal, Shallow Shallow, highly highly Shallow, Shoals and shorelines Shallow subtidal, subtidal, Shallow

c i t o i b A anhydrite pseudomorphs pseudomorphs anhydrite local cauliflower chert grains, peloids peloids grains, micritized grains grains, fullygrains, micritized coatings, micritized sand- cauliflower chert sized peloids; local peloids; sized oncolitic coatings, rare coatings, oncolitic oolitic coatings,thick micrite envelopes abundant cauliflower chert abundant afteranhydrite; rare calcite swallowtail gypsum flakes flakes common cauliflower chert pseudomorphs after cauliflower chert pseudomorphs after anhydrite anhydrite pseudomorphs after Peloidal matrix, common Peloidal Quartz silt to medium sand sand siltmedium Quartz to reworked Eolian, Peloids; common to common to Peloids; Quartz siltsand, mica and Oncolitic to oolitic cortices;oolitic Oncolitic to Peloids, coated grains; pisoids Soil Soil (l) 0 Abundant peloids;Abundant common Peloids, coated grains, fully Common oncolitic oolitic, Clotted micrite, coated Component ), coral heads,

c i t o i B Syringapora Syringapora eger and Read (1991), (k) intertidal, (l) supratidal. fragments, brachiopods, bryozoa, echinoderms, forams, trilobites F9) F9) Chaetetes, matrix similar toand F8 encrusting) common mollusks mollusks common encrusting) brachiopods, bryozoa, solitary bryozoa, brachiopods, trilobites corals, echinoderms, forams, shells, forams, bryozoa, fusulinids, articulated echinoderms; mollusk heads coral Syringapora solitary corals trilobites and and trilobites corals solitary and sponges molds; rare chaetetes, rhizoliths and redoximorphic root echinoderm fragments,bryozoa, and fusulinids haloes ostracodes; rare thin-walled ossicles, and solitary corals bryozoa, fusulinids fusulinids bryozoa, (spines), bryozoa, crinoids(spines), bryozoa, Mostly coral fusulinids, nuclei: as Tabulate corals ( Tabulate Abundant foramsAbundant (commonly Fusulinids, Fusulinids, Few: phosphatic brachiopods, Those of overprinted limestone facies; Common whole brachiopod valves and Rare thin-walled brachiopods, abraded Brachiopods (spines), trilobites; rare Common largefusulinids, brachiopods

y TABLE 4. SHELF INTERIOR FACIES d n a s

, y dolomitized packstone variably grainstone chert nodules t l i dolomite, chert chert dolomite, packstone, variable nodules carbonate Argilisols, and palimpsest abundant Vertisols cement/matrix brachiopods, abraded echinoderm packstone, variably cauliflower chert wackestone, and packstone cherty S Wackestone and Calcisols, Protosols, Grainstone to Dolomudstone, Dolomudstone, Framestone, Local cauliflower Local Dolowackestone and Boundstone and 1973), (i) Harris (1979), (j) Osl —laterally linked hemispherical; FWWB—fair weather wave base. (a) Above FWWB, (d) within photic zone, (e) Purser and Evans Evans and Purser (e) zone, FWWB,photic within (d) Above (a) base. wave FWWB—fair weather hemispherical; —laterally linked Sedimentary structures Sedimentary Lithology bioherms and biostromes stratified stratified troughs diameter, <30 cm high, cm high, <30 diameter, quartzand lime sand in unknown synoptic relief; wave ripples ripples wave stratification common, rare rare common, stratification local grainytraction deposits local grainytraction deposits granular cracks, soil pisoids; granular slickensides ped structure, horizonation, mudcracks, crinkly with LLH LLH with crinkly mudcracks, structures peloids/skeletal grains, grains, peloids/skeletal stromatolites,filland cut laminations of mud and Typically thoroughlybioturbated, Typically thoroughlybioturbated, Locally millimeter laminated Siltstone with

Roots, glaebules, circum- Planar tabular to trough cross- Micriticcm 1-5 thrombolite, Planar tabular cross- Planar millimeterPlanar centimeter to color scale; blue- scale; to meterto gray to tan scale beds; beds; scale blue blue scale; blue, to meter gray, tan meter scale tan or massive; reddish, reddish, or massive; centimeter centimeter scale meter scale gray to tan meter scale; brown Decimeter Decimeter locally blue locally blue yellow-red- tan Decimeter- scale; tan, Massive; tan Massive; tan Decimeter- meter- diameter to Centimeter Centimeter decimeter Decimeter to to Decimeter Massive; Decimeter to to Decimeter Massive; tan Massive; tan Rare millimeter lamination with Dolomudstone Irregular Irregular : G/P—pack-grainstone;: W/P—wacke-packstone; LLH Note W/P W/P photozoan (S17b) carbonate photozoan sandstone W/P (S17) (S17) W/P (S21) (S21) (F19) (F19) (1973), (g) Hagan and Logan (1974), (h) Loreau and Purser (h) ( Hagan and Logan (1974), (g) (1973), (S16c) (S16c)

framestone (S16d) (S16d) (S22) yellowish(S22) (S16b) (S16b) G/P (S16) Dolomitized Dolomitized Massive silty Lagoonal Lagoonal Paleosol (S20) (S20) Paleosol Centimeter to Coated G/P G/P Coated Dolomudstone Calcareous Calcareous Metazoan Laminite (S18) (S18) Laminite to Centimeter Thrombolite Thrombolite Facies Bedding and Facies Bedding Photozoan

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stromatolites, thrombolites, fusulinids, colonial and the variably restricted photozoan wacke- Outer-Ramp Facies corals, and dasyclad and other green algae, as packstones, laminites, and restricted siliciclastic well as most grains common to the heterozoan facies deposited in their lee. By late Pennsylva- Outer-ramp lithofacies (Table 1) consist of assemblage (e.g., James, 1997). nian time, the Bird Spring platform had evolved fi ne-grained carbonates common in uppermost Outer-ramp lithofacies consist of mud- and into a shelf, and shelf interior facies were depos- Chesterian to Desmoinesian (Serpukhovian to calcisilt-rich heterozoan carbonates that were ited in Arrow Canyon. These facies consist of Moscovian) strata, and siliciclastic mudstones deposited largely below the infl uence of storm more open photozoan pack- grainstones and common in upper Chesterian (Serpukhovian) waves. Middle-ramp lithofacies consist of het- more restricted, variably dolomitized wacke- strata. Outer-ramp facies include marls (OR1), erozoan and photozoan wacke-packstones that packstones, evaporative dolomudstones, and wavy interbedded cherts and calcisiltites (OR2), were deposited from storm wave base (SWB) laminites. They refl ect deposition in shelf inte- and massive to laminated calcisiltites (OR3) to fair weather wave base (FWWB). Inner- riors that were episodically restricted, highly (Fig. 2). These fi ne-grained carbonates have ramp facies consist of pack-grainstone shoals evaporative, and aggraded to sea level. a calcisiltite or mud matrix, common spicule

A B

500 µm 500 µm C D

E

100 µm

Figure 2. Outer-ramp, middle-ramp, and inner-ramp facies common in lower to middle Pennsylvanian strata. (A) Heterozoan grainstones: typical paucity of soluble aragonite grains inhibits later cementation and leads to fracturing and stylolitization (arrow) during burial (A118–1.0). (B) Heterozoan wackestone with brachio- pod and echinoderm fragments (A263–1.3). (C) Cross- 500 µm stratifi ed calcisiltite with low angle truncation (arrow) (A163). Pen is 15 cm long. (D) Calcisiltite showing bio- clastic and peloidal silt (A125). (E) Wavy interbedded calcisiltite and chert, showing common sponge spicule molds (arrows) in limestone, suggesting that chert beds were derived from spicule silica remobilized during early diagenesis (A293–0.4).

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molds, and where identifi able a heterozoan deposited in unrestricted waters, seaward of Inner-ramp siliciclastic lithofacies consist of assemblage of fossils. skeletal banks and coated grain shoals, as sug- irregular beds and lenses of variably calcare- Outer-ramp lithofacies were deposited below gested by their normal marine fl ora and fauna, ous, quartz sand and silt (IR15) that commonly SWB, delineated by lime mud- and silt-sized general lack of early dolomitization, absence of occur above fl ooding surfaces and exposure particles, the absence of photozoan grain types, evaporite pseudomorphs, and the progressive horizons. The thickest, in Atokan strata (A220), and an abundance of planar lamination. SWB in shoaling of these muddy carbonates into grainy is ~4 m thick, consists of planar to low-angle this interior seaway is estimated as between 30 ones within generally regressive meter-scale cross- laminated calcareous siltstone, and occurs and 60 m, based on modern analogs (e.g., Logan packages (see following cycle discussion). between a caliche and an outer-platform sulfi dic et al., 1969, 1970; Purser and Evans, 1973). An marl. An earliest Morrowan siliciclastic sandstone abundance of chert and spicule molds in these Inner-Ramp Facies also occurs as an ~1-m-thick massive siltstone to facies suggests that they formed in nutrient-rich very fi ne sandstone with root haloes developed in waters, possibly associated with upwelling from Inner-ramp facies consist of higher-energy its upper surface (A57). the Keeler Basin (see following). facies (pack-grainstones, thrombolites, meta- High-energy inner-ramp facies are inter- Outer-ramp siliciclastic lithofacies (Table 1) zoan framestones, cross-bedded sandstones) preted as shoals, skeletal banks, patch reefs, and consist of millimeter- to centimeter-scale, lami- deposited above FWWB, as well as the lagoonal more rarely, grainy foreshore deposits. Photo- nated, quartz silt- and clay-rich mudstones, restricted facies deposited in their lee (lagoonal zoan and heterozoan pack-grainstones were with rare marine fossils (IR4). Siliciclastic-rich wacke-packstones, tidal laminites, laminated deposited near and above FWWB (~7–20 m; deposits occur primarily in upper Chesterian siltstones). They are common throughout Osag- Logan et al., 1969, 1970; Purser and Evans, strata and likely record regional siliciclastic ean to Desmoinesian strata. 1973; Gischler and Lomando, 2005), as indi- infl ux derived from the Antler highlands to the Higher-energy facies are subdivided into cated by a common lack of carbonate mud and, west or the craton to the east (Poole and Sand- heterozoan, photozoan, and siliciclastic facies in many photozoan facies, coated grains. These berg, 1991; Trexler et al., 2004). The absence (Table 3). Heterozoan pack-grainstones (IR9) grainstone shoals, framestones, and bound- of cross-stratifi cation suggests that these facies have a heterozoan assemblage of fossils, locally stones typically formed breaks behind which were deposited in quiet water, below FWWB a calcisilt or muddy matrix, and are common in low-energy inner-ramp facies accumulated. and likely below SWB, possibly on a distal delta Osagean to Desmoinesian strata. High-energy Heterozoan and photozoan wacke- packstones front (Bishop et al., 2009). photozoan facies consist of skeletal, oolitic and/ are interpreted as lagoonal deposits based on or oncolitic and/or peloidal pack-grainstones a diverse fl ora and fauna and their position Middle-Ramp Facies (IR10), thrombolitic boundstones (IR10b), between high-energy facies and peritidal facies and metazoan framestones (IR10c). Metazoan in generally regressive meter-scale cycles (see Middle-ramp lithofacies (Table 2) are divided framestones are typically surrounded by grain- following). Thick and cryptmicrobial laminites into gently cross-stratifi ed calcisiltites (MR5), stones or less commonly wackestones, implying (F14) were deposited on lower and upper inter- heterozoan wacke-packstones (MR6), and pho- baffl ing of wave energy. Thrombolites are cut by tidal fl ats, respectively (e.g., Hardie and Shinn, tozoan wacke-packstones (MR7). These facies channels fi lled with grainstones, suggesting ener- 1986; Elrick and Read, 1991). are abundant in Morrowan to Desmoinesian getic environments, likely proximal to sea level Siliciclastic lenses (IR15) are common at strata. Cross-stratifi ed calcisiltites (MR5) have (e.g., Osleger and Read, 1991). High-energy cycle bases and are interpreted as lowstand gentle truncation surfaces that locally approach inner-ramp siliciclastic lithofacies consist of pla- deposits reworked during transgressions in hummocky cross-stratifi cation. Heterozoan nar tabular to trough cross-stratifi ed sandstones the platform interior. Their occurrence above wacke-packstones (MR6) have a heterozoan (IR8) that form thin-bedded to massive units, up subtidal fl ooding surfaces as well as exposure assemblage of fossils and a calcisiltite and/or to 5 m thick, in the upper Chesterian. horizons, coupled with their sedimentary struc- muddy matrix. Photozoan wacke-packstones Low-energy inner-ramp facies consist of tures, suggests a variety of transport mecha- (MR7) have photozoan grain types, a matrix lagoonal wacke-packstones, cryptmicrobial to nisms (eolian, fl uvial, shallow marine). Local composed of locally peloidal lime mud, and thick-laminites (IR13), and various siliciclas- pin-stripe lamination with subtle truncation in lack the evaporites and early dolomitization tic facies (IR15). Lagoonal wacke-packstones the thick lower Atokan example (A220) sug- common to inner-ramp and shelf interior photo- rarely have a heterozoan fauna (IR11) and more gests the local preservation of primary eolian zoan wacke-packstones. commonly a photozoan (IR12) one, which can sedimentary structures. The concentration of Gently cross-stratifi ed calcisiltites are inter- be partially dolomitized (IR12b). siliciclastic sediments at cycle bases suggests, preted to refl ect deposition at or near SWB. Peritidal facies consist of millimeter-scale for lowstands and early transgressive phases, Wacke-packstones are interpreted to have been cryptmicrobial laminites and millimeter- to either a proximal source only available episod- deposited below FWWB (7–20 m, Logan et centimeter-scale thick-laminites (IR13). ically, systematic changes in (eolian?) trans- al., 1969, 1970; Purser and Evans, 1973; Gis- Cryptmicrobial laminites consist of even to port direction or strength, or less dilution due chler and Lomando, 2005), where mud was crinkly millimeter-scale laminae of variably to a diminished carbonate factory. The early not winnowed by waves or currents, and above peloidal dolomudstone, with sparse mudcracks Morrowan massive siltstone to very fi ne sand- SWB (30–60 m; Logan et al., 1969; Purser and and laterally linked hemispherical stromato- stone (A57) is interpreted as an eolian deposit Seibold, 1973), where laminae of sand-sized lites. Thick-laminites consist of millimeter- to due to its uniform grain size and root haloes grains were deposited but subsequently largely centimeter-scale graded laminations of peloids developed in its upper surface. obscured by bioturbation. Photozoan lithofacies and lime mud with sparse mudcracks. Both are also constrained by the depth of the pho- cryptmicrobial and centimeter-scale thick- Shelf Interior Facies tic zone, estimated to be ~30 m in this muddy laminites are locally cut by decimeter-scale interior seaway (cf. Purser and Seibold, 1973; channels with coarse, intraclast-rich fi ll (cut- In mid-Desmoinesian through early Virgil- Foster et al., 1997). All of these sediments were and-fi ll structures). ian time, shelf interior facies were deposited in

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Arrow Canyon (Table 4). Shelf interior litho- fabrics of silicifi ed former anhydrite as well domorphs, and the succession of dolomitized facies consisted of variably coated photozoan as encapsulated dolomite rhombs that predate muddy facies above high-diversity grainy lime- pack-grainstones, thrombolites, and metazoan compaction (Fig. 3B). Swallowtail pseudo- stones within regressive meter-scale cycles (see framestones (S16), undolomitized (S17) to dolo- morphs of blocky calcite after gypsum are also following). Thick packages of homogeneous mitized (S17b) photozoan wacke- packstones, rarely present. dolomudstone (S19), lacking bedding surfaces dolomudstones (S19), cryptmicrobial to thick- Siliciclastic facies occur as thin irregular and with common to abundant caulifl ower laminites (S18), and various siliciclastic facies beds and lenses, which occur at fl ooding sur- chert (some with encapsulated aphanocrystal- (S21, S22). These facies are generally similar to faces (S21). In addition, in Desmoinesian strata line to fi ne crystalline dolomite rhombs) indi- those of the older inner ramp, described above. (A380), a 12-m-thick calcareous sandstone cate long-lived concurrent dolomitization and Notable distinctions are generally more abun- occurs (the Tungsten Gap chert); it has local pla- displacive anhydrite growth under unchanging dant synsedimentary dolomitization, especially nar lamination and rare phosphatic brachiopods, depositional conditions. We interpret this facies muddy sediments, and evaporite pseudomorphs, and is used as a marker bed across the Arrow to have been deposited in highly restricted particularly in massive (up to 15 m thick) out- Canyon Range. shallow lagoons under an arid climate regime, crop exposures of homogeneous, peloidal, very Grain-dominated shelf-interior lithofacies where postdepositional dolomitization was poorly fossiliferous dolomudstone (S19), with (S16) were deposited in shallow, high-energy driven by seepage from overlying lagoonal common to abundant caulifl ower- and popcorn- settings on the shelf, where tidal or wave waters or refl ux from adjacent sabkah environ- chert (Fig. 3B). Replacement dolomites consist energy winnowed mud. Muddy shelf interior ments (e.g., Sears and Lucia, 1980; Kendall and of fi ne to very fi ne crystalline (15–60 µm), sub- lithofacies (S17, S17b, S18, S19) were depos- Skipwith, 1969; Montañez and Read, 1992a, hedral to euhedral turbid crystals with planar ited in shallow, generally restricted waters, as 1992b; Montañez and Osleger, 1993, 1996; boundaries. Caulifl ower- or popcorn-cherts are suggested by a low-diversity, restricted fauna, Lehmann et al., 1998, 2000). centimeter-scale nodules that consist of chert, large fusulinids, thin-walled brachiopods, pel- Silty carbonate lenses (S21) preserved at quartz, blocky calcite, dolomite, and felted oidal muddy matrix, common evaporite pseu- cycle bases are interpreted as lowstand deposits

A B

500 µm 500 µm

C D

Figure 3. Upper Pennsylvanian shelf interior facies. (A) Oolitic grainstone with common moldic ooids and thin isopachous calcite cement (A445–1.2). (B) Peloidal dolomudstone disturbed by large, displacive popcorn-chert nod- ule. The nodule contains turbid rhombs of dolomite (gray) and silicifi ed laths after anhydrite (white), lending it a felted fabric (arrows). The association of dolomite, anhydrite, and displaced lamination implies that anhydrite emplacement and dolomitization occurred concurrently during deposition and very shallow burial (A442–0.95). (C) Restricted dolomitic wackestone with cut-and-fi ll channel structure, fi lled with fusulinid tests (A475–0.5). Pen is 13 cm long. (D) Thick laminite with millimeter- to centimeter-scale lamination cut by desiccation cracks (arrows); ~11 cm of pen showing (A391–0.3).

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reworked during ensuing transgressions. The cant moldic porosity, which is commonly fi lled (Montañez and Read, 1992a, 1992b) arid tidal thick Desmoinesian calcareous sandstone by Fe-poor (pink staining), nonluminescent fl ats. The absence of an overlying lag, however, (Tungsten Gap Chert) likely formed in estuarine meteoric cements. At a very well developed suggests that these horizons could also have environments, on the basis of rare phosphatic lower Chesterian karst horizon, several episodes formed by subaqueous erosion. brachiopods, the paucity of unabraded normal of meteoric cementation and reworking occur; marine fossils, local fl at lamination, and the these have been interpreted to refl ect missed Pedogenically Altered Surfaces absence of indicators for subaerial exposure. sea-level beats and the landward merging of Pedogenic features are abundant in upper unconformities (Bishop et al., 2009). Chesterian strata, common in Morrowan strata, Signifi cant Surfaces and rare in Atokan, Desmoinesian, and Missou- Horizons of Meteoric Cementation rian strata. Pedogenic alteration occurs on both Signifi cant surfaces are used to delineate In Chesterian to Virgilian strata, meteoric carbonate and siliciclastic substrates and ranges meter-scale cycles. Five types of surfaces are cements fi ll primary and secondary porosity and from rooted horizons indicative of ephemeral observed in the Arrow Canyon succession, are commonly associated with extensive moldic plant colonization to mature paleosol profi les. including fl ooding surfaces (1) and four types porosity; many of these surfaces do not exhibit Rooted horizons are typically developed of subaerial exposure horizons: paleo-karst karst or pedogenic features. Calcite cements are on limestones and contain millimeter- to surfaces (2), meteorically altered surfaces all nonferroan (stain pink with Dickson’s solu- decimeter-scale roots that bifurcate downward. (3), pedogenically altered surfaces (4), and tion) and nonluminescent to dully luminescent. Roots are preserved as redoximorphic root defl ation surfaces (5). Subaerial exposure hori- They occur as micritic meniscus cements in pri- haloes, carbonate and Fe-Mn oxide rhizoliths, zons are common (n = 52) and are associated mary pores (Fig. 4D), as very fi ne to fi ne crystal- and cherty compressions or adpressions. Root with extensive moldic porosity in the underlying line equant calcites (crystal silt) that geopetally walls are commonly lined by carbonate and/or limestones (though this feature is not considered fi ll primary and secondary pores (commonly clay, and root casts are locally fi lled by mete- unequivocally diagnostic of exposure; Melim within rhizoliths; Fig. 4C), and as circumgranu- oric cements (Fig. 4B). Rooted horizons com- et al., 2002). Subaerial exposure horizons are lar isopachous cements with scalenohedral ter- monly also contain grains and clasts blackened abundant in Chesterian and Morrowan (Serpuk- minations and/or syntaxial overgrowths on echi- with Fe and Mn oxides. hovian and early Bashkirian) strata, common in noderm ossicles. Paleosols are distinguished and classifi ed Atokan and mid-Desmoinesian (upper Bash- Meniscus cements and geopetal crystal silt are according to Mack et al. (1993) on the basis kirian and Moscovian) strata, and rare in upper interpreted as vadose cements that formed dur- of their soil (ped) structure (fi ne granular to Desmoinesian to lower Virgilian (Kasimov- ing subaerial exposure (Dunham, 1969, 1971). angular blocky, platy, rhomboid), horizonation, ian and Gzhelian) strata. Flooding surfaces are Individual generations of vadose cements are slickensides, extent of development of redoxi- common throughout Meramecian to Virgilian not observed in successive cycles, suggesting morphic features, and evidence for transloca- (upper Visean to Gzhelian) strata. that these cements are related directly to overly- tion and accumulation of Fe and Mn oxides, ing cycle bounding surfaces. Nonferroan, non- phyllosilicates, carbonates, and organic mat- Flooding Surfaces luminescent circumgranular cements and syn- ter. Chesterian paleosols in the Indian Springs Flooding surfaces are recognized as abrupt taxial overgrowths on echinoderm ossicles are and lowermost Bird Spring Formations include contacts where more shoreward facies are ret- interpreted as phreatic cements that precipitated Argillisols, Calcisols, Vertisols, and Protosols rogradationally overlain by more basinward from oxidized meteoric waters (Bishop et al., (locally gleyed, ochric, or plinthitic), and were facies. These surfaces can be sharp, erosive, or, 2009). Unless phreatic meteoric cements appear described at length in Bishop et al. (2009) (see more rarely, gradational. Facies above fl ooding reworked, they are not considered diagnostic of also Richards et al., 2002; Barnett and Wright, surfaces are commonly enriched in insoluble subaerial exposure (i.e., they might have formed 2008). Paleosol development in the overlying material and locally have phosphatized grains. during subsequent unconformities). Vadose Pennsylvanian interval of the Arrow Canyon Flooding surfaces represent transgressions of meteoric cements are considered diagnostic of succession is limited to Calcisols (n = 3) and the shoreline and mark cycle tops in the absence subaerial exposure and can be the only indicator Protosols (n = 3). of subaerial exposure. of exposure, or can be associated with karsted, Three paleosols occur in Atokan and Mis-

rooted, and pedogenically altered horizons. sourian strata and are characterized by CaCO3 Karsted Horizons accumulation, occurring as irregular 1–20-cm- Microkarst and macrokarst horizons are Defl ation Surfaces thick locally blackened crusts that veneer bed-

developed on subtidal limestones in lower Ches- Four truncation surfaces are developed on ding planes. These crusts effervesce in H2O2, terian and mid-Desmoinesian strata. Microkarst highly restricted shelf interior dolomudstones in indicating a concentration of Fe and Mn surfaces are recognized as scalloped, pitted Missourian and Virgilian strata. These sharp sur- oxides. They contain teardrop-shaped pisoids bedding planes with less than a few centime- faces exhibit as much as 20 cm of relief, place less and laminations of silty carbonate (Fig. 4E). ters relief, whereas macrokarst is associated restricted photozoan grainstone and/or wacke- Carbonate rhizoliths are common and typi- with centimeter- to decimeter-scale potholes, packstones over highly restricted dolomudstones, cally have geopetal fi lls of crystal silt. One fi ssures, and dissolution pipes (Fig. 4). Karst and are not associated with secondary porosity, of these paleosols crops out in lower Atokan surfaces are commonly fi lled by sandy palimp- meteoric cements, or karst features. strata as a white micritic bed, with local brown sest carbonate, terra rosa, sand- to cobble-sized Truncation surfaces are interpreted as pos- discoloration. In thin section, this horizon con- lithorelicts, and/or millimeter- to meter-scale sible defl ation surfaces that formed during sea- tains glaebules, defi ned by abundant circum- rhizoliths (e.g., Bishop et al., 2009). Roots, level falls when highly restricted, dolomitized, granular cracks and rhizoliths (Fig. 4F). pebbles, and skeletal grains are commonly cher- evaporite-rich sediments were exposed and These paleosols are interpreted as Calcisols tifi ed and/or blackened with Fe and Mn oxides. defl ated by winds, as noted on modern (Shinn, because their most prominent feature is the

Beneath karst surfaces, limestones have signifi - 1983; Hardie and Shinn, 1986) and ancient accumulation of pedogenic CaCO3. Blackened

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A B

30 cm 500 µm C D

500 µm 500 µm

E F

500 µm 500 µm

Figure 4. Subaerial exposure features. (A) Karst surface (black line), with fi ll of sandy palimpsest grains and lithorelicts (arrow) (A355–0.5). (B) Photomicrograph of rhizolith, with laminated peloidal carbonate coating (A-0). (C) Root cast (black outline) with geopetal fi ll of crystal silt and a displaced intraclast (arrows). Upper part of root cast occluded by blocky spar (A-0). (D) Peloidal grainstone with molds after aragonitic grains; vadose cementa- tion indicated by bridging (black arrow) and meniscus (white arrows) micritic cements. Rare beach deposit at A83–0.5. (E) Stage 3-4 pisolitic calcrete (Machette, 1985). Teardrop-shaped pisoids are commonly microstalactitic (A460–1.2). (F) Calcrete with two generations of circumgranular cracks, defi ning dark brown (large arrows) and green-brown (small arrows) glaebules (A218–0.8).

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crusts record vadose meteoric processes and and photozoan (IR10) pack-grainstones that IR10) and are capped by exposure horizons are distinguished from modern outcrop patina commonly pass upward into lagoonal wacke- (Figs. 5 and 6). Disconformable subtidal cycles by the teardrop-shaped pisoids, which are ori- packstones (IR11, IR12, IR12b) and are in middle-ramp settings refl ect shallowing from ented perpendicular to bedding (rather than capped by tidal laminites (IR13) (Figs. 2D below FWWB to above sea level. modern-day “down”). Although the accumula- and 9). Generally, middle- to inner-platform In upper Pennsylvanian shelf interior set- tion of pedogenic carbonate on limestone par- peritidal cycles refl ect shallowing from near tings, disconformable subtidal cycles are ent material must be interpreted climatically FWWB to sea level. bounded by (possible) defl ation surfaces, with caution, these Calcisols likely refl ect a In late Pennsylvanian strata, peritidal and in one instance a caliche. In these cycles, subhumid to semiarid climate regime (Royer, cycles are preserved in shelf interior settings more open-marine photozoan pack-grainstones 1999; Gong et al., 2005). and are capped by tidal laminites (S18), with (S16) are overlain by muddy lagoonal facies One interval of upper Morrowan strata con- cycle bases of lagoonal photozoan wacke- (S17, S17b, S19) with stratigraphically upward tains three stacked, weakly developed brown to packstones (S17, S17b) that increase in increasing dolomite and evaporite pseudo- gray horizons with redoximorphic root haloes restriction upward (increasing mud, dolomite, morphs, and decreasing faunal diversity and and platy ped structure; they pass downward and evaporite pseudomorphs, and decreasing abundance (Fig. 7). These facies transitions into olive-brown wackestones with marine faunal diversity and abundance) (Figs. 7C and refl ect increasing restriction across the shelf, fossils. These are classifi ed as Protosols due 15). Rarely, cycle bases consist of photozoan culminating in truncation surfaces, which may to weakly developed soil features. No climate pack-grainstones (S16) that pass upward into represent defl ation. In shelf interior settings, interpretation can be made on the basis of these restricted lagoonal facies (S17b) and tidal exposure-capped cycles refl ect shallowing from immature soil profi les. laminites (S18). These cycles refl ect increas- above FWWB to above sea level. ing restriction due to aggradation and/or pro- METER-SCALE CYCLES gradation and the fi lling of accommodation, Conformable Subtidal Cycles from above FWWB to sea level. Facies are distributed stratigraphically into Conformable subtidal cycles are bounded by meter-scale progradational-retrogradational Disconformable Subtidal Cycles fl ooding surfaces and are common throughout packages, bounded by disconformities or Meramecian to Virgilian strata in Arrow Can- fl ooding surfaces. These packages are 15 cm to Disconformable subtidal cycles contain yon. Typically these cycles are composed of the 19.5 m thick, averaging 3.5 m; they are referred exclusively subtidal facies and are bounded on same internal lithofacies as disconformable sub- to as cycles because each represents one cycle their upper surface by a subaerial exposure hori- tidal or peritidal cycles, but they lack subaerial of retrogradation and progradation, despite zon. These cycles occur throughout the Arrow exposure horizons and tidal fl at facies. not always exhibiting a predictable succession Canyon succession, but are particularly abun- In outer-ramp settings, conformable subtidal of facies (cf. Wilkinson et al., 1997, 1998). dant in Chesterian and Morrowan strata (e.g., cycles contain marls (OR1) overlain by wavy These cycles are classifi ed according to their Figs. 5–7). interbedded chert and calcisiltite (OR2), mas- bounding surface and uppermost facies (i.e., In deposits that formed in outer-ramp set- sive to laminated calcisiltite (OR3), and cross- disconformities developed on peritidal sedi- tings, disconformable subtidal cycles contain stratifi ed calcisiltite (MR5). Cycle tops com- ments, disconformities developed on subtidal marls (OR1) that pass upward into wavy inter- monly contain a pack-grainstone deposit (IR9 sediments, and conformable fl ooding surfaces bedded chert and calcisiltite (OR2), massive to or IR10; similar to the transgressive deposit developed on subtidal sediments), and are fur- laminated calcisiltite (OR3), and cross-stratifi ed in disconformable subtidal cycles) that likely ther characterized by the dominant position of calcisiltite (MR5), and are capped by subaerial formed during the sea-level lowstand or early constituent facies on the platform (i.e., inner, exposure horizons. Exposure surfaces are com- transgression (Fig. 11). Such cycles refl ect middle, and outer ramp, or shelf interior). Rep- monly overlain by photozoan or heterozoan shallowing from below SWB to near FWWB. resentative facies belts and cycles for different pack-grainstone transgressive deposits (IR9, A few lower Desmoinesian cycles deepen intervals of time are shown in Figures 5–7. IR10) (Fig. 6). Individual disconformable sub- upward and consist of basal photozoan grain- Figures 8–15 show representative windows of tidal cycles commonly lack one or more of the stones (IR10) that pass upward into outer-ramp Arrow Canyon strata with outcrop photos and lithofacies in these ideal cycles (Fig. 11). In marls (OR1) and spiculitic calcisiltite (OR3), stratigraphic logs, and illustrate how facies and upper Chesterian strata of the Indian Springs and are bounded at their tops by hardgrounds signifi cant surfaces stack to form meter-scale Formation, exposure-capped cycles consist (i.e., omission surfaces) (A288–A296; cycles. (For a complete Arrow Canyon log, see of outer-ramp laminated siliciclastic mud- Fig. 13). These are analogous to a combina- Bishop, 2008.) stones (OR4) and inner-ramp heterozoan pack- tion of the give-up and catch-down cycles of grainstones (IR9); rooted horizons and paleosols Soreghan and Dickinson (1994), in that they Peritidal Cycles may be developed on either of the constituent refl ect the temporary drowning of the ramp facies (Fig. 8). In Morrowan strata, very thin before relative sea-level fall brings the seafl oor Peritidal cycles consist of subtidal lithofacies (<0.5 m) cycles consist of marls (OR1) overlain back within the zone of maximum production, capped by intertidal facies with sharp to erosive by heterozoan pack-grainstones (IR9) with root- resuscitating the carbonate factory. bounding surfaces. Peritidal cycles are common ing structures (Fig. 10). Outer-ramp exposure- In middle- to inner-ramp settings, subtidal in Meramecian and early Morrowan inner-ramp capped cycles indicate shallowing from below cycles contain heterozoan (MR6) or photozoan settings, and in late Desmoinesian to Virgilian SWB to above sea level (i.e., exposure). (MR7) wack-packstones that coarsen upward shelf interior settings (Figs. 5–7, 9, and 15). In middle-ramp settings, disconformable sub- into pack-grainstones (IR9, IR10; Figs. 10 Peritidal cycles in Meramecian and lower tidal cycles commonly contain either heterozoan and 14). These cycles also locally contain thin Morrowan rocks were deposited in inner- (MR6) or photozoan (MR7) wacke-packstones outer-ramp facies at their cycle bases (Fig. 12). ramp settings and consist of heterozoan (IR9) that pass upward into pack-grainstones (IR9, In middle-ramp settings, conformable subtidal

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Figure 5. (A) Osagean to lower Chesterian depositional profi le. Encrinite shoals (left) were likely coeval with more shoreward shallow photozoan sediments (right). G/P—pack-grainstone; W/P—wacke-packstone; FWWB—fair weather wave base; SWB—storm wave base. (B) Encrinites near the Meramecian-Chesterian boundary (late Visean), showing the initial subaerial exposure horizon marking the onset of glacioeustasy (Bishop et al., 2009). (C) Shal- low, photozoan sediments of Meramecian age, with tidal fl at facies and peloidal, locally oncolitic pack-grainstones. In key, LLH is laterally linked hemispherical. Scale in meters above the top of the Arrowhead Formation.

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cycles refl ect changes in relative sea level from Noncyclic Interval tinuous deposition between SWB and FWWB near SWB to near to above FWWB. (Bishop et al., 2009). In shelf interior settings, conformable subtidal Osagean (lower Visean) strata in the Yel- cycles have photozoan lime pack- grainstones lowpine Formation contain a noncyclic interval CARBONIFEROUS STRATIGRAPHIC (S16) at their bases, passing upward into consisting of ~60 m of massive, poorly bedded AND CLIMATIC RECORD increasingly restricted, dolomitized lagoonal echinoderm pack-grainstones (IR9). These car- photozoan wack-packstones (S17, S17b, S19; bonates are consistent with deposition adjacent Long-term Accommodation History Fig. 15). These cycles are bounded by fl ooding to stable echinoderm banks, which were com- surfaces and contain facies that increase in their mon during Mississippian time (Kammer and Long-term sedimentary accumulation rates degree of restriction upward, yet did not shallow Ausich, 2006). This interval contains no facies for Arrow Canyon demonstrate that local completely to intertidal depths. changes or exposure horizons, suggesting con- variations in accommodation from middle

Figure 6. Lower Pennsylvanian deposition. (A) Schematic showing profi le of distally steepened Bird Spring ramp with distribution of contemporaneous facies (see Tables 1–3). (B) Lower Atokan cycles with regressive outer- ramp facies successions and thin middle- to inner-ramp packstones, locally exposure capped. (C) Lower Atokan cycles with outer-platform bases and inner-ramp to subaerially exposed cycle tops. (D) Lower Morrowan mixed heterozoan-photozoan cycles capped by thick laminites with sharp to erosive bounding surfaces. Scale in both meters above the top of the Arrowhead Formation (large numbers) and Amoco numbers (A = 1.5 m) measured from the top of the Battleship Wash Formation. See Figure 5 for legend.

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Figure 7. Upper Pennsylvanian deposition. (A) Interpreted distribution of Bird Spring shelf interior facies. Cycles are commonly capped by either tidal fl at facies or by highly restricted lagoonal dolomudstones, but no cycles contain both facies. (B) Upper Desmoinesian strata consisting of photozoan W/P passing into photozoan G/P or locally framestone, and capped by exposure horizons or subtidal fl ooding surfaces, with thin sandy transgressive/lowstand deposits. (C and D) Missourian cycles of increasing restriction, with facies becoming more restricted upward (e.g., increased dolomitization, evaporite pseudomorphs, mud, and faunal restriction). Bounding surfaces are subtidal fl ooding surfaces, disconformities devel- oped on tidal laminites, or possible defl ation surfaces (A443–1.0). Scale in both meters above the top of the Arrowhead Formation (large numbers) and Amoco numbers (A = 1.5 m) measured from the top of the Battleship Wash Formation. See Figure 5 for legend and abbreviations.

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Figure 8. Upper Chesterian strata, south side of canyon. Lowermost limestone is the top of the Battleship Wash Formation (A-0). Cycles consist of mixed carbonate-siliciclastic outer- to middle-platform facies, bounded by subaerial exposure horizons. Cl—clay; f—fi ne; c— coarse; gr—gravel. (Scale in Amoco numbers [A = 1.5 m, measured from the top of the Battleship Wash Formation]). See Figure 5 for legend and additional abbreviations.

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Figure 9. Lower Morrowan strata, north side of canyon. Peritidal cycles (A-60 to A-71) give way to disconformable and conformable subtidal cycles, developed on outer- to middle- platform facies, suggesting an increase in the amplitude of relative sea-level fl uctuations upward. (Scale in Amoco numbers [A = 1.5 m, measured from the top of the Battleship Wash Formation].) See Figure 5 for legend and abbreviations.

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Figure 10. Mid-Morrowan strata, south side of canyon. Facies changes are unpredictable, with subtidal cycles bounded by fl ooding surfaces and subaerial exposure horizons. Sub- aerial exposure features developed in cycles with outer-, middle-, and inner-ramp facies, suggesting generally high-amplitude changes in relative sea level. (Scale in Amoco numbers [A = 1.5 m, measured from the top of the Battleship Wash Formation].) See Figure 5 for legend and abbreviations.

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Figure 11. Lower Atokan strata, south side of canyon. Cycles consist predominantly of outer- ramp cycle bases, juxtaposed against middle- and inner-ramp cycle tops, and bounded by subaerial exposure horizons or subtidal fl ooding surfaces. These features suggest moderate- to high-amplitude relative sea-level fl uctuations. (Scale in Amoco numbers [A = 1.5 m, measured from the top of the Battleship Wash Formation].) See Figure 5 for legend and abbreviations.

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Mississippian to end-Pennsylvanian time over- marily refl ect changes in the creation of accom- better-dated Eurasian sections (e.g., Gradstein whelmed the global eustatic signal in this depo- modation space, rather than how effi ciently it et al., 2004). In contrast, though global stages sitional setting. However, this locally controlled was fi lled (Fig. 16C). are more precisely dated, they are only loosely long-term accommodation trend provides a Figure 16C presents two accumulation defi ned in Arrow Canyon, and North America context in which to assess the nature of short- plots for Arrow Canyon, determined using the in general. Thus, both age models have consid- term relative sea-level fl uctuations. Long-term North American and Russian Platform (global) erable uncertainty. However, despite the two accumulation rates were calculated based on stages, respectively. The differences in accumu- plots differing in detail, they clearly document rock thickness per stage, constrained by the lation rates derive from the fact that, although a similar long-term history of variations in integrated biostratigraphic zonation (Appendix in Arrow Canyon the North American stages accommodation space in the study area during A) and calibrated to the Gradstein et al. (2004) are well constrained biostratigraphically, these the Carboniferous. time scale. Most cycles shoal above SWB, so stage boundaries are relatively poorly dated, Estimated long-term sediment accumulation changes in this long-term accumulation plot pri- relying on biostratigraphic correlations to rates (Fig. 16C) indicate that accommodation

Figure 12. Upper Atokan strata, north side of canyon. Cycles have outer-ramp bases and thick middle- to inner-ramp tops, bounded by subaerial exposure horizons, subtidal fl ood- ing surfaces, or rare laminites (yellow). Juxtaposed outer- and middle- to inner-ramp facies with rare exposure horizons suggest a time of moderate- to high-amplitude relative sea-level oscillations. (Scale in Amoco numbers [A = 1.5 m, measured from the top of the Battleship Wash Formation].) See Figure 5 for legend and abbreviations.

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Figure 13. Upper Atokan to lower Desmoinesian strata, south side of canyon. Cycles juxta- pose outer- and middle- to inner-ramp facies and are dominantly regressive. Several cycles are dominantly transgressive (e.g., A289–0.5, A293–0.5) and bounded by omission surfaces. Juxtaposed outer- and middle- to inner-ramp facies along with the absence of subaerial exposure horizons suggest moderate-amplitude relative sea-level fl uctuations. (Scale in Amoco numbers [A = 1.5 m, measured from the top of the Battleship Wash Formation].) See Figure 5 for legend and abbreviations.

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Figure 14. Middle to upper Desmoinesian strata, south side of canyon. This interval likely encapsulates the transition from distally steepened ramp to (locally) rimmed shelf (Miller and Heller, 1994), as indicated by the loss of outer- and middle-ramp storm-dominated facies (base of photo), common metazoan bioherms that shoaled to sea level (middle), and the advent of restricted evaporative dolomitic facies (upper). Subtidal cycles contain domi- nantly photozoan middle- to inner-platform facies with common subaerial exposure hori- zons, suggesting at least moderate-amplitude relative sea-level fl uctuations. Relatively thick cycles suggest either more effi cient fi lling of accommodation, likely associated with progra- dation and development of a platform margin, or greater accommodation creation (e.g., fourth- to fi fth-order cycles superimposed on a third-order transgression). (Scale in Amoco numbers [A = 1.5 m, measured from the top of the Battleship Wash Formation].) See Fig- ure 5 for legend and abbreviations.

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was twofold to tenfold higher during the Mor- Atokan maximum in accommodation occurs sylvanian, diminished subsidence sensitizes rowan through Missourian (20–70 m/m.y.) than during a eustatic second-order regression and/ the Arrow Canyon record to even moderate during the Chesterian (7 m/m.y.) or Virgilian or lowstand (Ross and Ross, 1987; Galonka amplitude high-frequency changes in relative (12.6 m/m.y.), with greatest accommodation and Kiessling, 2002). This suggests that long- sea level, which should cause exposure of the during the Atokan (68 m/m.y.) and Desmoines- term eustatic changes in this region were largely shallow subtidal facies. Thus, the Arrow Can- ian (59 m/m.y.). This long-term accommoda- superseded by local subsidence. It is this local yon section provides a window of opportunity tion history likely refl ects the combined effects increase in subsidence that allows for the pres- for capturing the full range of amplitudes of of changes in tectonically driven subsidence in ervation of mostly complete high-amplitude, relative sea-level change when the creation of the Keeler Basin and second- and third-order high-frequency cycles during the global sea- accommodation space is high (early to mid- (>1 m.y.) eustatic fl uctuations. Notably, the level lowstand. Similarly, during the late Penn- Pennsylvanian), and constrains the maximum

Figure 15. Upper Desmoinesian to Missourian strata, with cycles of increasing restriction, including thick packages of highly restricted lagoonal dolomudstone (e.g., A424–0.5–433– 0.5). Uniformly shallow water facies, rare disconformable subtidal cycles, and common per- itidal cycles suggest a time of low-amplitude relative sea-level oscillations. (Scale in Amoco numbers [A = 1.5 m, measured from the top of the Battleship Wash Formation].) See Fig- ure 5 for legend and abbreviations.

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M Chesterian Morrowan Atokan Desmoinesian Missourian V Bur. A Vis Serpukhovian Bashkirian Moscovian Kasimovian Gze. B 0 0 10 10 20 20 30 30 40 40 50 50 60 60 70 70 80 80 (m/m.y. =mm/mly.) (m/m.y. Accumulation Rate Accumulation 0 0

C 100 100

200 200

300 300

400 400

(k.y./cycle) 100

Avg. cycle duration cycle duration Avg. Paleosol

peritidal (tidal lam D 80 lagoon, restricted lagoon) photic (phot W/P, 60 phot G/P, phot lagoon) heterozoan (het G/P, het W/P) 40 deep subtidal (x-strat by facies (%) facies by calcisilt, calcisilt, chert/calcisilt, marl) Proportion of each cycle, 20 x-strat silic. sand

siliciclastic muds 0 100 E

80

60

40 SWB within each cycle OR1: marl OR1: OR3: calcisilt OR3: Range of inferred water depth change water Range of inferred FWWB 20 OR:2: chert/calcisilt OR:2: MR5: x-strat calcisilt x-strat MR5: F 0 MR6: het W/P het MR6: 5 W/P phot. MR7: OR4: siliciclastic muds OR4: (m) cycle IR9: het. G/P het. IR9: mean thickness thickness

Cycle type: peritidal cycle disconformable subtidal cycle conformable subtidal cycle sand x-strat IR8:

G G/P phot. IR10, S16: IR13, S18: laminite IR13, S18: S19: dolomudstone S19: IR10c, S16c: met FS S16c: IR10c, IR12b, S17b: dol phot S17b: IR12b, IR10b, S16b: thrombolite S16b: IR10b, IR 11, 12, S17, 22: lagoon IR 11, 12, S17, 22: IR10d, S16d: coated G/P IR10d, S16d: paleosol, eolian, exposure

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that sea level could have changed when accom- (Read et al., 1986; Read, 1995). Moderate- modation creation was lowered (late Pennsyl- to high-amplitude relative sea-level changes vanian), given that at such times accumulating should be recorded by (1) the juxtaposition of carbonates would be very sensitive to any high- facies from markedly different water depths in amplitude relative sea-level changes (i.e., tidal the same cycle, and/or (2) subaerial exposure fl ats would be stranded landward and syndepo- horizons developed on subtidal sediments. sitional dolomite would be limited; Read et al., Basinward settings may record more conform- 1986; Montañez and Read, 1992a). able subtidal cycles with juxtaposed outer- and Figure 16. Relative sea-level history for middle- to inner-platform facies, or disconform- Arrow Canyon, according to cycle number. Relative Sea-Level History able subtidal cycles. In contrast, shoreward set- (A) Carboniferous geologic stages, fi tted to tings should record cycles capped by subaerial cycle number using all available biostratig- The history of short-term relative sea-level exposure horizons developed on inner-platform raphy (Appendix A). (B) Long-term accu- fl uctuations is reconstructed using water depths facies due to overall lowered accommodation mulation curve, as a proxy for accommoda- inferred from the lithofacies in each cycle and coupled with forced regressions. tion. Rates estimated using North American the distribution of subaerial exposure horizons The record of relative sea-level change and (red) and global (black) stage boundaries. (Fig. 16). Ranges of water depths for each facies cycle bounding surfaces is depicted in Figure 16. (C) Average cycle period according to stage, are calibrated to inferred depths for FWWB, Four features are prominent and indicate shifts using North American (red) and global SWB, and the photic zone based on sedimen- between intervals of high-amplitude and low- (black) stage boundaries. (D) Proportion tary structures, grain types, and using modern amplitude short-term relative sea-level fl uctua- of cycle made up of each facies association. and ancient facies analogs (Tables 1–4, and tions, including (1) a Chesterian (late Visean) Upper Mississippian to middle Pennsyl- references therein). Comparisons between the onset of relative sea-level fl uctuations of moder- vanian cycles have prominent outer-ramp deepest and shallowest facies in each cycle ate to high amplitude; (2) a short-lived (earliest facies; Upper Pennsylvanian cycles are provide an estimated range of relative sea-level Morrowan or Bashkirian) dampening of relative dominated by shallow, restricted, and peri- change within that cycle. These depth ranges are sea-level changes and the development of peri- tidal facies. (E) Range of relative sea-level highly sensitive to inferred SWB and FWWB, tidal cycle caps; (3) a return to high-amplitude, change for each cycle, based on range of which can vary signifi cantly depending on geo- high-frequency relative sea-level changes in water depths inferred for the deepest and graphic setting. For this Carboniferous shallow the mid-Morrowan (early Bashkirian) to mid- shallowest water facies present in each interior seaway, SWB is inferred to be 40 m and Desmoinesian (late Moscovian); and (4) a cycle. Colored areas represent band of pos- FWWB to be ~20 m, although FWWB can be marked decrease in amplitude of late Desmoine- sible amplitudes, with highest confi dence considerably shallower (~8 m in the Persian sian to early Virgilian (Kasimovian to early Gze- in estimates less than the depth to storm Gulf; Purser and Evans, 1973; Gischler and lian) relative sea-level fl uctuations and a con- wave base (SWB) (shown in yellow). The Lomando, 2005) and SWB considerably deeper comitant return to dominantly peritidal cycles. range of estimates represents a minimum (~60 m in the Yucatan; Logan et al., 1969) on for cycles with facies deposited below SWB modern carbonate platforms. These values pro- Temporal Distribution of or with disconformable bounding surfaces vide a relatively conservative estimate of sea- Climatic Signatures (e.g., Chesterian-Desmoinesian). Estimated level changes. Amplitudes of sea-level change ranges bracket the maximum magnitude estimated beyond these wave-base thresholds Osagean and Meramecian (Visean) age strata for peritidal or conformable subtidal cycles are less well constrained; the maximum water contain ~65 m of noncyclic middle- to inner- with facies deposited above SWB (e.g., depth for deep subtidal sediments is arbitrarily ramp encrinites and ~15 m of photozoan inner- much of late Pennsylvanian). See text for defi ned as 100 m but could have been greater. ramp facies. Low-amplitude relative sea-level further explanation. FWWB—Fair weather Overall, the magnitudes of sea-level falls may changes are inferred because these strata con- wave base. (F) Long-term average cycle be underestimated where cycles are exposure tain only middle- to inner-ramp facies, with a thickness, as a proxy of subsidence per capped and/or contain facies that formed below long-lived noncyclic interval and conformable cycle. A more accurate estimate of eustatic SWB. However, for conformable subtidal or subtidal and peritidal cycles, lacking evidence amplitudes would subtract this thickness peritidal cycles with facies deposited entirely for exposure of subtidal sediments. Meramecian from the range in water depths inferred above SWB, these estimates capture the maxi- strata likely exhibit autocyclic behavior because from constituent facies. (G) Distribution of mum relative sea-level change, given the depths peritidal fl at facies do not correlate regionally cycle types. Intervals of low-amplitude rela- inferred for each facies. between Arrow Canyon and neighboring Battle- tive sea-level changes (in the Meramecian, Estimates of short-term relative sea-level ship Wash (Bishop et al., 2009). Fenestral tidal lower Morrowan, and upper Desmoinesian change, in concert with variations in the types fl at facies suggest a subhumid climate for this to Virgilian) are accompanied by more of cycle bounding surfaces, are indicative of time (e.g., Bova and Read, 1987; Hardie and common peritidal cycles. See Figure 5 for different climate states and glacioeustatic forc- Shinn, 1986). abbreviations. ing (Fig. 16G). In general, during times of low- The onset of moderate- to high-amplitude rel- amplitude glacioeustasy, basinward settings ative sea-level fl uctuations occurs 1 m above the develop amalgamated conformable subtidal Meramecian-Chesterian (late Visean) boundary cycles that show minimal facies changes or may (Bishop et al., 2009), where subaerial exposure be noncyclic. In shoreward settings, carbon- horizons are developed on subtidal encrinites and ates usually fi ll accommodation space, creat- (stratigraphically higher) on middle- to outer- ing fl at-topped platforms with peritidal cycles platform carbonates and siliciclastics (Figs. 5 that prograde extensively across the platform and 8). In upper Chesterian ( Serpukhovian)

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cycles, exposure horizons developed on middle- restricted, evaporative facies, common meta- scale peritidal cycles in proximity to faults (e.g., to outer-ramp siliciclastic mudstones record zoan bioherms, and the slightly younger devel- Cisne, 1986; Hardie et al., 1991). In particular, changes in relative water depth at least equiv- opment of Missourian phyloid algal bioherms the forward stratigraphic models of De Benne- alent to the depth of FWWB and likely SWB in western Nevada and Death Valley (Miller dictis et al. (2007) suggest that in extensional (>20–40 m; Fig. 16E). Notably, Chesterian and Heller, 1994). settings, peritidal cycles might be produced in Vertisols and calcic paleosols suggest that a sea- Upper Desmoinesian, Missourian, and lower the hanging wall or graben by episodic down- sonal dry subhumid to semiarid climate existed Virgilian (uppermost Moscovian to lower Gzhel- drop (causing rapid deepening) followed by minimally by this time (Bishop et al., 2009). ian) strata record a long-lived interval of low- to aggradation due to carbonate productivity. And Earliest Morrowan (earliest Bashkirian) possibly moderate-amplitude relative sea-level disconformable subtidal cycles might be pro- strata exhibit evidence for a short-lived mini- fl uctuations. These uniformly shallow-water, duced by episodic uplift of the footwall or horst mum in magnitudes of relative sea-level change photozoan facies accumulated under approxi- (causing rapid shallowing and subaerial expo- (Figs. 16E, 16G). The lower ~20 m of Mor- mately fourfold diminished accommodation. sure horizons) followed by slow background rowan strata consist of mixed heterozoan- The low accommodation and shallow-water subsidence, allowing the return of carbonate photozoan inner-ramp facies capped by thin deposition require that any moderate or high- production. De Bennedictis et al. (2007) docu- tidal fl at laminites; they contain only one thin amplitude relative sea-level fl uctuations would mented rates, frequencies, and magnitudes of (50 cm) incursion of outer-ramp facies (Fig. 9). generate exposure-capped cycles. However, slip that are consistent with many meter-scale The presence of tidal fl ats and rarity of outer- exposure horizons are rare—between 1 and 5 of carbonate cycles. ramp facies suggest low-amplitude relative 32 cycles, depending on whether truncation sur- The Arrow Canyon record of high-amplitude sea-level oscillations, during which the car- faces are interpreted as defl ation surfaces. This relative sea-level change (disconformable sub- bonate factory kept pace with transgressions, suggests a long-lived interval of low-amplitude tidal cycles) would require high-frequency excluding outer-ramp facies, and tidal fl at pro- high-frequency sea-level changes, punctuated normal faulting with large slips (>40–50 m) gradation kept pace with short-term regressions by rare moderate-amplitude sea-level changes. that persisted over a very long period of mid- (Read et al., 1986; Read, 1995, 1998). Given the rarity of exposure horizons and uni- Mississippian to mid-Pennsylvanian time Mid-Morrowan to mid-Desmoinesian (early formly shallow, subtidal to peritidal facies, the (~25 m.y.). However, this interval brackets Bashkirian to Moscovian) strata record signifi - range of relative sea-level change indicated in several different tectonic regimes on the west cantly higher-amplitude short-term sea-level Figure 16 thus represents a maximum. The reap- coast of North America (Trexler et al., 1991, changes (Figs. 16E, 16G). High-amplitude pearance of common tidal fl at-capped cycles 2003, 2004; Stevens and Stone, 2007). In addi- relative sea-level fl uctuations are demonstrated further supports generally low-amplitude fl uc- tion, such fault-controlled meter-scale cycles where exposure horizons are developed on these tuations, because even moderate sea-level falls require depressed carbonate productivity to dominantly outer-ramp cycles (Figs. 10–13). In would have caused shorelines to rapidly regress prevent “keep-up” peritidal conditions (during addition, rapid sea-level changes are required by across the low-relief platform interior, strand- the interval of slow background subsidence), the short cycle durations in this interval. A ten- ing any tidal fl ats that might have formed dur- which would preclude deep subtidal facies. fold decrease in average cycle duration occurs ing sea-level stillstands (e.g., Read et al., 1986; Otherwise, the resulting disconformable cycles during the Atokan maximum in accommodation Read, 1995, 1998). The presence of cycles would consist entirely of peritidal carbonate (Fig. 16C). In part, this decline in cycle dura- with thick (15 m) accumulations of highly facies. Most important, Arrow Canyon discon- tion refl ects the ability of deeper water facies to restricted lagoonal dolomudstones at other formable subtidal cycles require both abrupt record most high-amplitude sea-level changes, times during this interval suggests the occur- sea-level rises (commonly >40 m at the base of and thus minimize missed beats. However, rence of sea-level changes of low to moderate each cycle) and abrupt sea-level falls (because some of the change in cycle duration likely also amplitude; large enough to generate (possible) cycle thickness is much less than maximum refl ects changes in sea-level forcing (e.g., from defl ation surfaces in some cycles and to prevent recorded water depth), culminating in exposure the 100 k.y. eccentricity to the 40 k.y. obliq- tidal fl at complexes from prograding across of the platform. Such a relative sea-level history uity band). Atokan strata include two caliches the highly restricted, shallow lagoons, but low requires both forced transgressions and regres- (Figs. 4F and 11) and a thick, reworked silici- enough to allow long-lived accumulation of sions, inconsistent with the structural model clastic eolianite (at approximately A220), sug- these restricted facies without triggering facies presented here. Moreover, the absence of seis- gesting continuation of an overall dry subhumid changes. In addition, a Missourian calcisol, mites and growth faults and the relatively large to semiarid climate regime. abundant concurrent dolomitization and evapo- (~200 km) distance from Arrow Canyon to the Relative sea-level changes diminished rite emplacement (Fig. 3B), and a paucity of major Keeler basin fault system (Stevens and in amplitude during the late Pennsylvanian meteorically altered surfaces attest to a marked Stone, 2007) do not support a structural origin (Fig. 16). During a mid-Desmoinesian (upper aridifi cation during this time. for these cycles. Rather, abundant evidence for Moscovian) transitional interval, amplitudes of Upper Virgilian and Wolfcampian strata are coeval glaciation in Gondwanan records (see relative water-depth change decrease markedly, heavily recrystallized, masking depositional following discussion) implicates glacioeustatic yet middle- to inner-ramp cycles are bounded and early diagenetic textures, and obscuring the forcing for these medium- to high-amplitude by subaerial exposure horizons (Fig. 14). relative sea-level record for this interval; there- relative sea-level changes. These exposure-capped cycles suggest forced fore, environmental, sea-level, and climatic con- In contrast, intervals of low-amplitude rela- regressions under at least moderate-amplitude ditions are not interpreted from these strata. tive sea-level change (dominantly peritidal relative sea-level fl uctuations. In addition, this and conformable subtidal cycles) are consis- interval likely corresponds to the development Tectonic Control of Meter-Scale Cycles tent with structural, autocyclic, or eustatic of a (rimmed) shelf to the west. This transition origins (e.g., Hardie et al., 1991; Burgess, is recorded by the loss of storm-dominated It has been suggested that “jerky” subsid- 2001; De Bennedictis et al., 2007; Bosence outer- to middle-ramp facies, increasingly ence or “yo-yo” tectonics might produce meter- et al., 2009). Regardless of the predominant

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cause, however, such intervals cannot have volume history, consistent with the variable immediately above the Meramecian-Chesterian been characterized by high amplitudes of gla- glaciation inferred from high latitudes. This boundary (Bishop et al., 2009); this discon- cioeustasy (see following). conclusion demands a more nuanced view than formity is interpreted to mask several of the the prevailing low-latitude model of persistent high-amplitude glacioeustatic events inferred Implications for Reconstructing high-amplitude glacioeustasy caused by the pro- from the midcontinent (Bishop et al., 2009). the Late Paleozoic Record of Ice Volume tracted waxing and waning of a long-lived, geo- Thus, the onset of glacioeustasy inferred from graphically expansive late Paleozoic ice sheet. the Arrow Canyon succession is consistent The paleo-tropical mixed carbonate- In Arrow Canyon, basal Chesterian strata with previously published near- and far-fi eld siliciclastic succession at Arrow Canyon pro- record the onset of high-amplitude relative sea- records. This high-amplitude glacioeustasy vides substantial insights into Carboniferous level fl uctuations and inferred glacioeustasy continues until just above the Mississippian- low-latitude climate dynamics (Fig. 17). In other (Bishop et al., 2009). This is slightly later than Pennsylvanian boundary. low-latitude settings, persistent high-amplitude the onset of glaciogenic sedimentation in South In lowermost Morrowan (lowermost Bash- (30 to >150 m) glacioeustasy throughout middle America (Caputo et al., 2008), but predates kirian) strata, common tidal fl at cycle caps and Mississippian to early Permian time has been evidence of glacial sedimentation elsewhere in a paucity of intercalated outer-ramp facies sug- extrapolated from the relief on unconformities Gondwana (Isbell et al., 2003a; Fielding et al., gest a minor short-lived glacial minimum, or and juxtaposed facies in cyclothems, and the 2008a, 2008b). Tropical estimates for the onset a large but stable ice sheet (DeConto and Pol- geochemical records of their biotic compo- of glacioeustasy range from late Meramecian lard, 2003). This time period corresponds with nents (e.g., Heckel, 1977, 1986, 1994; Adlis et (mid-Visean) to late Chesterian (late Serpukho- an interval of normal fl uvial and/or lacustrine al., 1988; Horbury, 1989; Soreghan and Giles, vian) time but tend to converge near the base sedimentation across eastern Australia (Fielding 1999a; Smith and Read, 2000; Wright and Van- of the Chesterian (upper Visean) (Bishop et al., et al., 2008a, 2008b), which was near the polar stone, 2001; Cook et al., 2002; Joachimski et 2009). Variability in these records is likely due circle at the time, more consistent with a time of al., 2006). In contrast, high-latitude sedimentary to differing subsidence regimes and positions limited glacial extent. Such short-lived minima records suggest multiple, smaller ice sheets that on platforms, causing different sensitivities to have been attributed to fourth-order sea-level waxed and waned to varying degrees at different eustatic sea-level changes, as well as possible cycles superimposed on third-order sea-level times, leading to alternating long-lived intervals limitations in biostratigraphic constraints and highstands (Read, 1995), consistent with dimin- of glacial maxima and minima (Isbell et al., intercontinental correlation. Soon after the ished glacioeustatic forcing during times of 2003a, 2003b, 2008a, 2008b; Montañez et al., onset of glacioeustasy, repeated fl uvial incision smaller ice sheets. 2007; Fielding et al., 2008a, 2008b; Caputo et in the midcontinent suggests high-amplitude The mid-Morrowan to mid- Desmoinesian al., 2008). The low-latitude Arrow Canyon suc- (>30–85 m) relative sea-level fl uctuations interval of inferred high-amplitude gla- cession preserves a record of shifting modes (Smith and Read, 2000). In Arrow Canyon, a cioeustasy is consistent with both low-latitude of glacioeustasy that suggests a dynamic ice- potentially long-lived disconformity occurs and high-latitude records, which suggest this as

335 330 325 320 315 310 305 300

Mississippian Pennsylvanian Pe. Period Visean Serpukhovian Bashkirian Moscovian Kasim. Gzelian As. Global stage Meram. Chesterian Morrowan Atokan Desmoin. Miss. Virgil. Burs.Wo. N. Amer. stage Battleship Wash Indian YP Gap ? Gap Springs Bird Spring Formation Bird Spring/Keeler Basin (pull-apart from sinistral truncation of Inherited Antler Foredeep Tectonic setting N. America or part of Ancestral Rockies) Ramp: (Rimmed) Shelf: phyloid algal Ramp: Ramp: mixed Distally Steepened Ramp: photo- margin, evaporative platform Platform type echinoderm-dominated carb-clastic Storm dominated zoan interior Heterozoan & Mixed Photozoan- Photo- Heterozoan Photozoan ? Sediment type zoan Siliciclastic Het. Heterozoan fenestral (calcic) Vertisols, Protosols Calcisols, Calcisol, evaporites & Climatically sens- tidal flats Argillisol, Lycopsid mire Protosols dolomites itive sediments Seasonal, subhumid to Climatic Subhumid? Seasonal, semiarid Arid ? ? semiarid signature high Long-term med accommodation low high Magnitudes of ? ? med ? ? relative sealevel low change Magnitude uncertain Peak Min Peak Minimum Miss. mod. or ? ? Glaciation ? ? ? ? stable Pennsylvanian ice

ice Max ?

Figure 17. Summary of stratigraphic and climatic trends derived from Arrow Canyon record. Time scale after Gradstein et al. (2004).

Geosphere, Februrary 2010 27

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a time of peak Carboniferous ice (e.g., Veevers latitude records (e.g., midcontinent cyclothems) nary open-ocean models of gentle thermoclines, and Powell, 1987; Frakes et al., 1992; Isbell et have traditionally been interpreted to refl ect absent haloclines, and buffered tropical climates al., 2003a; Fielding et al., 2008a). In addition, high-amplitude glacioeustasy. However, few of (glacial-interglacial changes in sea-surface the abundance of cherty heterozoan limestones these interpretations are based on quantifi able temperature of 1–4 °C) to Pennsylvanian shal- with molds after sponge spicules, horizons with evidence for sea-level change (e.g., erosional low epeiric seas. However, these epeiric seas scattered phosphatized grains, and a subhumid relief at lowstands). Rather, in upper Missou- would have been especially prone to sluggish to semiarid climate (see following) suggests rian to lower Virgilian strata, erosional relief mixing of water masses (e.g., Holmden et al., upwelling of cool, nutrient-rich waters onto the on disconformities demonstrates only low- to 1998; Panchuk et al., 2005, 2006), large salin- Bird Spring platform during this interval (cf. moderate-amplitude (20–40 m) incision events ity fl uctuations (e.g., >8 ppt across the Bahamas Pope and Steffen, 2003). (Feldman et al., 2005). Only two records sug- platforms; Patterson and Walter, 1994), shallow Relative sea-level changes in upper Desmoi- gest high-amplitude (60–70 m) sea-level fl uc- pycnoclines (Algeo and Heckel, 2008), and the nesian through lower Virgilian strata suggest tuations, based on fl uvial incision at lowstands. development of subtle intrashelf depressions an interval of signifi cantly diminished mag- Both intervals, however, occur just below the (e.g., where black shales form in shallow Meso- nitudes of relative sea-level fl uctuations. It is Desmoinesian-Missourian boundary (Schenk, zoic basins; Immenhauser and Scott, 2002; during this interval, one traditionally attributed 1967; Heckel et al., 1998). Furthermore, reex- Homewood et al., 2008). For example, depleted to peak icehouse conditions, that the greatest amination of some analogous later Virgilian δ18O in conodont apatite deposited during high- disparity exists between many near- and far- “classic” incised valleys has resolved multiple stands is interpreted to represent signifi cantly fi eld records. In eastern Australia, late Penn- superimposed lower-amplitude incision events, diminished ice caps (Joachimski et al., 2006). sylvanian strata contain none of the glacio- reducing inferred eustatic magnitudes from However, interglacial temperature changes genic sediments or evidence of high-amplitude >60 m to <30 m (Fischbein et al., 2009). beyond the 2–4 ºC assumed by Joachimski et al. relative sea-level fl uctuations that typify other The paradigm of high-amplitude late Des- (2006) would have a signifi cant effect on gla- glacial intervals (Fielding et al., 2008a, 2008b, moinesian to early Virgilian glacioeustasy cioeustatic estimates; e.g., an extra ~2 ºC cool- 2008c). Rather, these strata record normal is derived primarily from facies changes in ing would offset 40–50 m of inferred sea-level marine and fl uvial conditions, with only mod- Kansas-type cyclothems (Heckel, 1977, 1986, change. Indeed, to the degree that such epeiric est relative sea-level changes. Similarly, Ant- 1994; Boardman and Heckel, 1989). In these seas buffered continental temperatures, the arctic records indicate nonglaciated basement cyclothems, exposure horizons are juxtaposed seas’ temperatures would have been perturbed highs on which thick paleosols developed and against phosphatic black shales that accumu- (Stanley, 2006). Accordingly, evidence for that were onlapped by postglacial strata (yet lated below a pycnocline. The inferred depth of near-freezing tropical surface waters (Brand- were not eroded by subsequent ice sheets), the pycnocline (>50–90 m) provides the funda- ley and Krause, 1994, 1997) and low-latitude precluding the existence of a large ice sheet mental constraint on relative sea-level change, low-altitude alpine glaciation (Soreghan et al., over Antarctica (Isbell et al., 2003a, 2003b, leading to glacioeustatic estimates of >100 m 2008) suggests a dynamic tropical climate with 2008b). These ice-free basins were polar, indi- (Heckel, 1977, 1994). This model is based on episodically cold, shallow waters. Joachimski cating a largely ice-free southern pole during thermocline depths estimated from modern et al. (2006) utilized a static salinity structure this interval (Montañez et al., 2007; Fielding et ocean basins, and requires the absence of any for the midcontinent sea, assuming no change al., 2008a, 2008b, 2008c; Isbell et al., 2008b). haloclines across the much more restricted between glacial and interglacial settings. This In subpolar settings, Desmoinesian to Virgilian midcontinent epeiric sea. However, such tropi- premise would be remarkable given the episod- ice is currently reported from several basins: cal seas would be highly sensitive to changes ically stratifi ed water column (punctuated by the Paraná, Karoo-Kalahari, the Arabian Pen- in runoff and the creation of shallow haloclines black shale deposition). Specifi cally, Joachim- insula, and possibly the Congo (Rocha-Cam- (e.g., Algeo and Heckel, 2008; Algeo et al., ski et al. (2006) compared conodonts deposited pos et al., 2008; Holtz et al., 2008; Isbell et al., 2008). Indeed, the organic matter content and nearshore during lowstands with those depos- 2003a, 2008a; Stollhofen et al., 2008; Martin geochemistry of “core” shales in midcontinent ited offshore during highstands. Algeo and et al., 2008). However, ice fl ow directions in cyclothems now support such a shallow (15– Heckel (2008) inferred salinity gradients of these basins require multiple ice sheets (e.g., 30 m) halocline (Algeo and Heckel, 2008). In 10‰ within the stratifi ed midcontinent epeiric Isbell et al., 2008a), likely at least fi ve to seven addition, in the Visean paleo-equatorial Mount sea, with highstand surface waters diluted by (J. Isbell, 2008, personal commun.). The Head Group of Canada, glendonites (pseudo- increased continental runoff. Using a modern absence of an ice sheet over Antarctica and morphs after thinnolite) record near-freezing equatorial Atlantic analog (Fairbanks et al., eastern Australia and the presence of multi- temperatures in shallow-marine facies, suggest- 1992), this salinity change would cause a 1‰ ple smaller ice sheets in lower latitude basins ing very shallow thermoclines in this tropical δ18O depletion, offsetting ~100 m of inferred place important constraints on continental ice interior seaway (Brandley and Krause, 1994, sea-level change (Joachimski et al., 2006). It sheet volume and possible amplitudes of gla- 1997). In concert, this evidence for shallow might be argued that lateral salinity gradients cioeustasy. Given the same aerial extent, multi- (15–30 m) Carboniferous epeiric sea pycno- would lead to lower salinity during lowstands ple smaller ice centers can lock up signifi cantly clines indicates that “core” shales might have due to deposition more proximal to the shore- less water than one large ice sheet (Isbell et formed at shallow depths and magnitudes of line and presumed freshwater input. However, al., 2003a), leading to greatly dampened gla- glacioeustasy may have been signifi cantly less it is only during highstands in the midcontinent cioeustasy. Thus, the late Pennsylvanian gla- (~15–30 m) than commonly inferred. that evidence exists for stratifi ed water columns cioeustatic minimum inferred from Arrow In a similar fashion, high-amplitude (>70– (black shale deposition, rather than the steno- Canyon strata corresponds with a time of lim- 120 m) glacioeustatic fl uctuations have been haline fauna and oxygenated bottom waters ited glacial extent in high-latitude Gondwana. reconstructed from oxygen isotopic changes of transgressive and regressive limestones; During the inferred upper Desmoinesian to within cyclothems (Adlis et al., 1988; Joachim- Algeo and Heckel, 2008). Furthermore, mid- lower Virgilian glacial minimum, other low- ski et al., 2006). Such estimates apply Quater- continent paleosols and coal deposits imply a

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semiarid to subhumid climate during lowstands vasive recrystallization, which obscures many In the Arrow Canyon record, the coincidence and a humid to subhumid climate during early depositional characteristics. of signifi cantly more arid conditions with the transgressions, possibly sustained through decline in amplitude of glacioeustasy argues highstands (e.g., DiMichelle et al., 2010, and Aridifi cation for a strong component of climate forcing, sug- references therein). Joachimski et al. (2006) gesting a mechanistic link between pantropi- assumed that the conodont-bearing organism The Arrow Canyon record indicates a cal aridifi cation and the retreat of high-latitude did not respond to changing environmental marked aridifi cation during the proposed late Gondwanan ice sheets. conditions; however, there is much uncertainty Pennsylvanian glacial minimum, a signature regarding where in the water column conodont- recorded elsewhere across equatorial western CONCLUSIONS hosting organisms lived and how they adapted to Pangea (Rankey, 1997; West et al., 1997; Olsze- changing temperature, salinity, nutrient inputs, wski and Patzkowski, 2003), equatorial eastern The record of glacioeustasy archived in and oxygenation. Thus, the assumptions that Pangea (DiMichele et al., 2009, and references Arrow Canyon requires a much more dynamic modern thermocline profi les would be operable therein), and high-latitude western Gondwana Carboniferous glaciation than commonly per- in late Pennsylvanian seas (Adlis et al., 1988), (Gulbranson et al., 2010). This late Pennsyl- ceived. This record is at odds with the prevailing that glacial-interglacial tropical temperature vanian aridifi cation is coincident with mass view that cyclothems require high-amplitude changes in the Pennsylvanian were comparable extinctions of tropical peat-forming lycopsids glacioeustasy throughout the ~50 m.y. interval to those of the Pleistocene (Joachimski et al., (DiMichelle and Phillips, 1996) and a concomi- of their deposition. The Arrow Canyon record 2006), and that haloclines would not be oper- tant change in the quality of Appalachian coal is more consistent with high-latitude records able, may be grossly oversimplifi ed in these (Cecil et al., 2003). that suggest alternating long-lived intervals of geochemical models. It is commonly held that arid tropical condi- glacial maxima and minima, including a late Even within the Euramerican cyclothem tions were coincident with icehouse intervals Desmoinesian–early Virgilian glacial mini- record, a more nuanced interpretation is emerg- during the Paleozoic. This conclusion is largely mum. This late Pennsylvanian minimum was ing. Rygel et al. (2008) compiled published based on extrapolating climate changes on coincident with a marked aridifi cation in Arrow estimates of glacioeustatic magnitudes; they short time scales (<105 yr; glacial-interglacial) Canyon and across the tropics, supporting a link showed that these reported estimates (of varying based on Pleistocene analogues to longer time between high-latitude ice sheet extent and sta- vintage and veracity) delineate broad patterns of scales (106 yr; icehouse-greenhouse). Thus, evi- bility and ocean-atmospheric dynamics in the fl uctuating magnitudes through the late Paleo- dence for arid glacials and humid interglacials tropics (e.g., Poulsen et al., 2007). zoic. More specifi cally, Heckel (2008) revisited has been extrapolated to require arid icehouse These climatic oscillations had a signifi cant his classic cyclothem interpretation to conclude intervals and humid greenhouse intervals. In impact on the facies, cyclicity, and stacking pat- that the majority of the late Pennsylvanian Permian time, however, aridifi cation of the terns in Arrow Canyon. The recognition of a cyclothem record actually refl ects highstands tropics was coincident with long-lived green- dynamic late Paleozoic ice age suggests that not in long-term sea level and thus corresponds to house intervals during the fi nal phase of the all cyclothems formed under the same glacioeu- diminished ice volume over Gondwana: these late Paleozoic ice age (Montañez et al., 2007). static forcing, and should lead to a much more intervals include many of the major and inter- During the late Pennsylvanian, aridifi cation of nuanced understanding of late Paleozoic tropi- mediate cyclothems, for which the largest gla- western equatorial Pangea (and withdrawal of cal sedimentation. cioeustatic magnitudes have been inferred. This the epicontinental seas) has been linked to the analysis again reinforces that the cyclothems of fi nal assembly of Pangea and thermotectonic ACKNOWLEDGMENTS the midcontinent, and the meter-scale cycles of buoyancy of the supercontinent, mechanisms We thank Mike Eros, Neil Kelley, and Erik Arrow Canyon, are not one size fi ts all, a simple independent of ice sheet dynamics (Veevers, Gulbranson for fi eld assistance, and Paul Brenckle, repeated motif. Rather, they vary in character, 1994; Ziegler et al., 2002). However, this expla- Greg Wahlman, and Vladimir Davydov for biostrati- and this variability refl ects the dynamic nature nation is confounded by a marked aridifi cation graphic expertise. Blaine Cecil, Mitch Harris, Scott of late Paleozoic glaciation. east of the main Pangean tropical mountain belt Ritter, and Lynn Soreghan provided advice and dis- Numerous authors have interpreted inci- (DiMichele et al., 2009). Climate models sug- cussion. Scot Franklin, Tom Brady, James Sippell, Mark Boatwright, and Cathy Wiley all helped arrange sion of 30–50 m in upper Virgilian carbon- gest that aridifi cation during glacial minima access and sampling permits. We also thank Norm ates (Wilson, 1967; Goldstein, 1988; Rankey was caused by a weakening of Hadley cell con- Winter and Greg Baxter for analytical and laboratory et al., 1999), and Soreghan and Giles (1999a, vection and southward drift of the Intertropi- support. The clarity and focus of this manuscript were 1999b) documented >30–85 m of relief on cal Convergence Zone, leading to decreased improved considerably by detailed reviews from Tom Algeo, Andrew Barnett, and associate editor Kate some unconformities. However, in Arrow precipitation levels and intensifi ed monsoonal Giles. This work was supported by National Science Canyon, late Virgilian relative sea-level circulation across western equatorial Pangea Foundation grant EAR-0545654 (Sedimentary Geol- changes are diffi cult to interpret due to per- (Poulsen et al., 2007; Montañez et al., 2007). ogy and Paleontology Program) to Montañez.

Geosphere, Februrary 2010 29

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s s e e e v , n n o b o . s s n n n a e f e e a a . m r m r a a a e L C A Baesemann and Lane (1985); et al.Lane (1999) 198.3 (A64-1.3) Amoco: Groves and Miller, Bishop 2000; et al., Amoco: Groves and Miller, V. 2000; Davydov, 2007, personal Langenheimal. et (1984) Amoco: Groves and Miller, Baesemann 2000.; and Lane (1985) 275 (A116) L commun.. L Amoco: Groves and Miller, V. 2000; Davydov, 2007, personal commun. CassityLangenheim and (1966); Amoco: Groves and Miller, 2000 436 (A223-0.5) Baesemann and Lane (1985); et al. Lane (1999) 198.8 (A65-0.3) Brenckle (1997);Brenckle al.et (1997);al.et (1999)Lane 101 (A0) B L W A C B commun. C

n

a a i l i n u g r a i f

V

r

) f o

o Eoschubertella

a e r Adetognathus Adetognathus lautus s o l a and F b

porcatus and

s Beedeina e t a (= (= m i x o

r . APPENDIX A. BIOSTRATIGRAPHIC ZONATION IN ARROW CANYON p APPENDIX A: BIOSTRATIGRAPHIC ZONATION IN ARROW CANYON ARROW IN ZONATION A: BIOSTRATIGRAPHIC APPENDIX A . p Gnathodus bilineatus, G. girtyi birdspringensis minutus minutus minutus minutus Asteroarchaediscid foraminifers; foraminifers; Asteroarchaediscid N “Millerella” tortula tortula “Millerella” Rhachistognathus muricatus Profusulinella decora decora Profusulinella Fusulina Declinognathodus noduliferus Schwagerina Schwagerina Apotognathus Fusulinella Fusulinella Profusulinella spicata spicata Profusulinella Adetognathodus unicornisAdetognathodus Idiognathodus suciferus Pseudofusulinella utahensis, Triticites A Neognathodus symmetricus Pseudostaffella R. muricatus muricatus R. Triticites burgessae variousforaminiferaand conodonts Oketaella Cecil etal. (2003);Stamm and Wardlaw (2003) 634 (A355-0.5) Idiognathoides sinuatus; Rhavhistognathus

e n o Z

. . A A . . 10 (bilineatus) Cyclothem Cyclothem N N Base of Lower Kittanning

n

a i

n m a u i l s e r z u A# is Amoco (A prefix) location number; N.A.—not available. Stratigraphic height given in metersArrowhea above the top of the

G B s

l l e a a g s s a Note: a a t Basal Chesterian Undifferentiated FUand 9 Basal Bashkirian Basal FU (Noduliferus)15 Upper Serpukhovian FU 12 (Unicornis) Upper Serpukhovian FU 13 (Lower Muricatus) Basal Serpukhovian B Late Meramecian FU 8 2000,” and is followed by a reference to any reinterpretation of those data. the top of Battleship Wash Formation, and bed numbers Cassity Langenheim, 1966. Amoco data archived in universit Basal Desmoinesian Lower Bashkirian Bashkirian Lower Sinuatus-Minutus Symmetricus B Asselian Basal N.A. Upper Serpukhovian FU 14 (Upper Muricatus) Upper Atokan Atokan Upper Fusulinella Basal Moscovian Moscovian Basal Basal Atokan Atokan Basal Atokan Mid Profusulinella Missourian Tricites Desmoinesian: Desmoinesian: Lowermost Kasimovian N.A. Basal Missourian Missourian Basal N.A. S Basal VirgilianBasal N.A.

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