Detrital Zircon Record of Mid-Paleozoic Convergent Margin Activity in the Northern U.S

RESEARCH

Detrital zircon record of mid-Paleozoic convergent margin activity in the northern U.S. Rocky Mountains: Implications for the Antler orogeny and early evolution of the North American Cordillera

Luke P. Beranek1, Paul K. Link2, and C. Mark Fanning3 1DEPARTMENT OF EARTH SCIENCES, MEMORIAL UNIVERSITY OF NEWFOUNDLAND, 9 ARCTIC AVENUE, ST. JOHN’S, NEWFOUNDLAND AND LABRADOR A1B 3X5, CANADA 2DEPARTMENT OF GEOSCIENCES, IDAHO STATE UNIVERSITY, 921 SOUTH 8TH AVENUE, POCATELLO, IDAHO 83209, USA 3RESEARCH SCHOOL OF EARTH SCIENCES, AUSTRALIAN NATIONAL UNIVERSITY, 142 MILLS ROAD, CANBERRA, ACT 0200, AUSTRALIA

ABSTRACT

The passive to convergent margin transition along western Laurentia drove early development of the North American Cordillera and culminated with the Late Devonian–Mississippian Antler orogeny and emplacement of the Roberts Mountain allochthon in the western United States. New detrital zircon studies in the Pioneer Mountains, east-central Idaho, were conducted to investigate the stratigraphic evidence of this transition and test models for mid-Paleozoic tectonics and paleogeography. Ordovician to Lower Devonian passive margin strata of the Roberts Mountain allochthon and adjacent North American parautochthon contain ca. 1850, 1920, 2080, and 2700 Ma detrital zircons that indicate provenance from the Peace River Arch region of northwestern Laurentia. These detrital zircons are much older than the depositional ages of their host rocks and probably record long-term sediment recycling processes along the Cordilleran margin. Upper Devonian strata, including Frasnian turbidites of the Roberts Mountain allochthon, document the incursion of 450–430 Ma and 1650–930 Ma detrital zircons from an unknown source to the west. Detrital zircon Hf isotope results suggest that the western source was an early Paleozoic arc built on Proterozoic crust, with the Eastern Klamath, Northern Sierra, and Quesnellia terranes as likely candidates. Lower Mississippian syntectonic strata filled a rapidly subsiding, releasing bend basin that was associated with sinistral-oblique plate convergence and reworking of lower Paleozoic rocks in east-central Idaho. The available detrital zircon and stratigraphic data are most consistent with noncollisional models for the Antler orogeny, including scenarios that feature the north to south, time-transgressive juxtaposition of Baltican- and Caledonian-affinity terranes along the Cordilleran margin.

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INTRODUCTION mid-Paleozoic to Cenozoic tectonothermal events (e.g., Dickinson, 2004, 2006; Nelson et al., 2013). Studies of mid-Paleozoic plate convergence have Accretionary orogenic systems are built by repeated tectonothermal mostly focused on components of the Late Devonian–Mississippian Antler events that construct mountain belts over tens to hundreds of millions of orogeny in the Great Basin of Nevada, which culminated in lower Paleozoic years (e.g., Cawood et al., 2009). Field evidence for the oldest tectonic deep-water rocks of the Roberts Mountain allochthon (Fig. 1) (western events in such long-lived orogens can therefore be obscured by later assemblage of Roberts et al., 1958; siliceous assemblage of Burchfiel and phases of deformation, metamorphism, and magmatism that effectively Davis, 1975) being thrust over carbonate platform strata (eastern or carbon- rework the continental crust. However, it is widely accepted that ancient ate assemblage) of the Laurentian margin (Nilsen and Stewart, 1980; John- siliciclastic strata are important archives of early orogen processes and son and Pendergast, 1981; Poole et al., 1992). Outside of the Great Basin, capable of retaining the precise age, spatial extent, and exhumation his- a protracted history of plate convergence is further evidenced by Middle tories of old mountain belts (Allen et al., 1991; Ross et al., 2005; Weis- to Late Devonian arc magmatism, metamorphism, and deformation (e.g., logel et al., 2006; Cawood et al., 2007; Anfinson et al., 2013; Gehrels, Mortensen, 1992; Root, 2001; Dusel-Bacon et al., 2006) and Late Devonian– 2014; Colpron et al., 2015; McClelland et al., 2016). Detrital mineral Early Mississippian backarc extension, syngenetic sulfide mineralization, provenance studies of syntectonic strata have proven to be especially and syntectonic sedimentation (e.g., Eisbacher, 1983; Gordey et al., 1987; useful for identifying the geological elements that supply clastic detritus Miller et al., 1992; Turner and Otto, 1995; Nelson et al., 2006; Diehl et to sedimentary basins during convergent margin activity, such as passive al., 2010) in parts of the Alaskan, Canadian, and United States Cordillera. margin sequences, cratonal blocks, and volcanic arcs (Clift et al., 2009; Mid-Paleozoic backarc extension ultimately led to the rifting of continental Hampton et al., 2010; Park et al., 2010; LaMaskin, 2012; Beranek et al., arc fragments and opening of a marginal ocean basin along western North 2013a, 2015; Bradley and O’Sullivan, 2016; Zhang et al., 2016). America (Creaser et al., 1997; Piercey et al., 2004; Colpron et al., 2007). The Cordilleran orogen of western North America (Fig. 1) is the type Three plate tectonic scenarios are typically proposed to explain the Ant- example of an accretionary system and has a documented history of ler orogeny: (1) the collision of an east-facing arc system of Laurentian or

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non-Laurentian crustal affinity against the west-facing Cordilleran passive margin (e.g., Burchfiel and Davis, 1972; Schweickert and Snyder, 1981; Speed and Sleep, 1982; Dickinson et al., 1983a); (2) the noncollisional closure of a marginal basin between a generally west-facing arc and the Cordilleran margin (e.g., Burchfiel and Davis, 1972; Poole, 1974; Burch- Arctic fiel and Royden, 1991; Miller et al., 1992); and (3) the dextral (Wright Alaska and Wyld, 2006) or sinistral-oblique (Colpron and Nelson, 2009) juxta- RB position of non-Laurentian crustal blocks against the Cordilleran margin. KB AG Limited provenance constraints have hampered attempts to test these FW scenarios and identify the geological elements involved in mid-Paleozoic convergent margin activity. For example, it remains an open question if Devonian–Mississippian syntectonic strata preserved along the length of the Cordilleran orogen were in part sourced from arc complexes of the a Eastern Klamath, Northern Sierra, and Quesnellia terranes (Fig. 1) that Alask ukon WR Y may have originally developed near Baltica or West Gondwana (Wright YT and Wyld, 2006; Grove et al., 2008; Colpron and Nelson, 2009, 2011). Sediment provenance studies in Nevada concluded that Antler foreland North American basin and overlap strata are mostly composed of detrital zircons older than continental margin SM 1800 Ma derived from Laurentian affinity rocks of the Roberts Mountain Platformal strata Yukon BC allochthon (e.g., Gehrels et al., 2000a). Basinal strata Detrital zircon provenance studies of mid-Paleozoic strata outside the Terranes of western Great Basin are required to establish new ideas on early orogen paleoge- Laurentian a nity Quesnellia, Stikinia (ST), AX ography and the erosional history of the Antler mountain belt. A primary other early Mesozoic arcs candidate for study is the Pioneer Mountains region of east-central Idaho McCloud, Redding, Klinkit/Harper Ranch, Stikine ST (Figs. 1 and 2) that contains western and eastern assemblage passive mar- ta gin rocks, mid-Paleozoic syntectonic strata, and upper Paleozoic overlap BC Yukon-Tanana (YT) er

AlAlberb successions that were juxtaposed together during the Mesozoic Sevier Slide Mountain (SM) CC WR SM orogeny (Roberts et al., 1958; Nilsen, 1977; Mahoney et al., 1991; Poole Terranes of Siberian, Baltican, and Sandberg, 1991; Wilson et al., 1994; Link et al., 1995). For example, & Caledonian a nities some Cenozoic fluvial sands and Middle Pennsylvanian Sun Valley Group Alexander (AX) Quesnellia strata in the Pioneer Mountains yield ca. 470–380 Ma and 1650–930 Ma Arctic Alaska, Ruby (RB) Purcell Mtns. detrital zircons that were likely recycled through Antler belt rocks (Link OK Farewell (FW), Kilbuck (KB) et al., 2005, 2014; Beranek et al., 2006). These detrital zircon populations CanaCanada Okanagan (OK), Trinity-Yreka (TY) United StatesStatda are not typical of western Laurentian strata, including Paleozoic strata of Sierra City-Shoo Fly (SC) es the Roberts Mountain allochthon (Gehrels and Pecha, 2014; Linde et al., Terranes of northern WA 2016), and therefore bring into question the crustal provenance of rock Panthalassic a nity OR units in the Antler highland. To investigate this problem, we acquired the Angayucham (AG), Tozitna Figure 2A Wrangellia (WR) detrital zircon U-Pb signatures of Ordovician–Lower Devonian passive Eastern margin strata (Kinnikinic Quartzite, Basin Gulch Quartzite Member of Terranes of Tethyan a nity Klamath TY the Phi Kappa Formation, Cait quartzite of the lower Milligen Forma- Cache Creek (CC), Bridge River ID tion), Middle to Upper Devonian strata (Independence sandstone of the Baker, Rattlesnake Creek SM NV UT upper Milligen Formation, Jefferson Formation), and Mississippian Antler SC Roberts Mtn. foreland basin strata (Copper Basin Group, Salmon River assemblage) 0 500 Northern allochthon Sierra in the Pioneer Mountains region. New Hf isotope data are reported to km further constrain the provenance of dated zircons in the Milligen Forma- NV CA tion (this study) and Sun Valley Group (Link et al., 2014). The results allow us to document the transition from passive to convergent margin tectonics along western North America and identify the geological elements involved in mid-Paleozoic plate convergence. In combination with published information, we present models for Paleozoic paleogeography that can be tested by future studies.

PALEOZOIC STRATIGRAPHY OF THE PIONEER MOUNTAINS, Figure 1. Paleozoic to early Mesozoic terranes of the North American Cor- IDAHO dillera modified from Colpron and Nelson (2009). Terranes are grouped according to crustal affinity and interpreted positions in early Paleozoic time. Outlined box shows the geographic location of Pioneer Mountains Paleozoic rocks in the Cordilleran thrust belt of east-central Idaho region in Figure 2A. BC—British Columbia, CA—California, ID—Idaho, NV— crop out within three structural-stratigraphic zones that from west to Nevada, OR—Oregon, UT—Utah, WA—Washington. east comprise the Pioneer, Copper Basin, and Hawley Creek thrust plates (e.g., Link and Janecke, 1999). Cambrian to Devonian strata to the east of the Pioneer thrust (Fig. 2A) consist mostly of shallow-water, platformal

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Pioneer Copper Basin Hawley Creek Challis Explanation thrust plate thrust plate thrust plate A . Penn.-Permian Sun Valley B Group and equivalents Mississipian Copper Basin Group and equivalents Permian Sun Valley Gp. White Cloud Peaks Devonian Milligen Formation 03PL12 04TD10 Snaky Cambrian to Devonian Canyon Fm. 24PL09 continental margin strata Salmon Pennsylvanian 01PL12 River 05TA09 Detrital zircon sample locality

. Lost River Range Hawley Creek 05PL13 thrust plate 09LR01 Copper White Knob Basin Gp. Limestone 44° 00’ N Mississippian Copper Basin Big thrust plate Lost 24PL09 River 10 & 40JMP94 McGowan 05PL15 Creek Fm. Boulder 06PL13 05PL15 Mountains 09LB04 Pioneer Pioneer . 09LB04 C Mackay 05PL13 thrust plate opper Mountains Independence ioneer thrust P

11LB04 opper Basin thrust 04TD10 Basin Je erson Fm. C Je erson Fm. Devonian Milligen Fm. thrust

09TD10 . Cait 02TD10 Ketchum 02TD10 40JMP94 Big Wo . 10JMP94 11LB04I Silurian Trail Creek Fm. Mt. Rob. Fm. Laketown Dol. P ionee od Kinnikinic Kinnikinic

r Quartzite Quartzite River Phi KKaappappa Fm. Hailey thrust Ordovician 09TD10 09LR01 . 06PL13 05TA09 01PL12

03PL12 02km 0 Cambrian Wilbert Fm. Wilbert Fm. 114° 00’ W

Figure 2. (A) Simplified bedrock map of the Pioneer Mountains region, east-central Idaho, modified from Lewis et al. (2012). White circles show the location of detrital zircon samples reported in this study. Penn.—Pennsylvanian. (B) Cambrian to Permian correlation chart for the Hawley Creek, Copper Basin, and Pioneer thrust plates. Detrital zircon samples are shown by white circles and sample numbers. Dol.—Dolomite, Fm.—Formation, Gp.—Group, Mt.—Mount, Rob.—Roberts.

rocks of the Cordilleran passive margin (eastern assemblage of the North Ordovician to Silurian siliciclastic rocks of the Phi Kappa and Trail American parautochthon) that are assigned to the Sauk, Tippecanoe, and Creek Formations comprise continental slope and rise facies of the Cordil- Kaskaskia sequences of the North American craton. The Ordovician Kin- leran passive margin (western assemblage of the Roberts Mountain alloch- nikinic Quartzite (Fig. 2B) is a prominent siliciclastic unit in east-central thon) that crop out to the west of the Pioneer thrust fault (Figs. 2A, 2B). Idaho and broadly correlative with the Eureka Quartzite of eastern Nevada The Phi Kappa Formation, and in particular its basal Basin Gulch Quartzite that is beneath the Roberts Mountain allochthon. Ketner (1968) con- Member, is correlative with the shallow-water Kinnikinic Quartzite of cluded that quartz-rich Ordovician sand sheets in the western United States east-central Idaho and the deep-water Valmy and upper Vinini Formations were sourced from the Peace River Arch, a long-lived positive feature in of the Roberts Mountain allochthon in Nevada. For example, the basal northwestern Alberta and northeastern British Columbia (e.g., O’Connell Phi Kappa Formation contains Ordovician hexactinellid sponges that are et al., 1990; Cecile et al., 1997), and transported southward along the similar to those in the Vinini Formation (Rigby et al., 1981; Rigby, 1995) Cordilleran shelf by longshore processes. This hypothesis is supported and likely diagnostic of the warm water paleo-Pacific realm (Carrera by the increased textural maturity of Ordovician shelf sandstones from and Rigby, 1999). Although it is generally agreed that Roberts Mountain western Canada to the southwestern United States (e.g., Ketner, 1968) allochthon strata have Laurentian provenance, there has been consider- and Precambrian detrital zircon signatures that are consistent with north- able debate about the origins of some deep-water Ordovician rocks in west Laurentian provenance (e.g., Gehrels and Ross, 1998; Baar, 2009; the Great Basin (see Gehrels et al., 2000a). In one popular scenario, tex- Wulf, 2011; Gehrels and Pecha, 2014). Shallow-water quartz sandstone turally immature sandstones of the upper Vinini and Valmy Formations units also occur throughout the carbonate-dominated Devonian Jefferson have provenance ties with the Peace River Arch region of northwestern Formation within the Copper Basin and Hawley Creek thrust plates (Fig. Laurentia and were deposited in offshelf environments near their pres- 2B), including Famennian strata in the Lost River Range near Borah Peak ent locations; lower Vinini Formation strata in this scenario were derived (Grader and Dehler, 1999). from nearby source regions in southwestern Laurentia (e.g., Smith and

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Gehrels, 1994; Gehrels et al., 1995, 2000a). Linde et al. (2016) modified conglomerates contain cherty argillite rock fragments that suggest prov- this hypothesis and proposed that upper Vinini and Valmy strata were enance from western assemblage Phi Kappa and Milligen strata of the deposited offshore of the Peace River Arch, near the latitude of the pres- Roberts Mountain allochthon (Link et al., 1996). East of the Pioneer ent day U.S.-Canadian border, and subsequently transported ~1000 km Mountains, distal turbidite (McGowan Creek Formation) and carbonate south by a sinistral strike-slip fault system prior to the Antler orogeny. (White Knob Limestone) successions of the Hawley Creek thrust plate Devonian Milligen Formation strata are limited to the Pioneer thrust (Figs. 2A, 2B) were deposited at the boundary between the eastern margin plate (Figs. 2A, 2B) and comprise >1000 m of variably deformed black of the Antler foreland basin and the western edge of the cratonal platform. shale, chert, sandstone, conglomerate, mafic sills, and tuff. The Milligen Middle Pennsylvanian to lower Permian siliciclastic-carbonate marine depocenter was a restricted marine basin that received clastic input from rocks of the Sun Valley Group and Snaky Canyon Formation (Fig. 2B) unknown sources to west and the Cordilleran shelf to the east (Turner compose the Antler overlap succession in east-central Idaho (e.g., Mahoney and Otto, 1988). As outlined by Link et al. (1995), a general sequence of et al., 1991; Geslin, 1998). In the Pioneer thrust plate, Sun Valley Group events for the Milligen Formation includes (1) Early Devonian (Emsian) rocks unconformably overlie deformed Milligen Formation strata. Link et deposition of the east-derived Cait quartzite member; (2) Middle to Late al. (2014) reported that Sun Valley Group strata yield Archean to Paleozoic Devonian (Eifelian to Frasnian) deposition of the Triumph argillite mem- detrital zircons with key age groupings ca. 1840, 1750, 1650, 1450, 1150, ber during localized extensional faulting and exhalative mineralization; 1040, 650, 565, and 440–415 Ma. Although these provenance signatures and (3) Late Devonian (Frasnian) deposition of the west-derived Inde- are similar to other Pennsylvanian–Permian strata in the northern U.S. and pendence sandstone member. The Milligen Formation locally contains southern Canadian Rocky Mountains (e.g., Gehrels and Pecha, 2014), it an Antler age penetrative cleavage that is not observed in younger strata is uncertain if some detrital zircons, including ca. 440–415 Ma zircons, of the Pioneer Mountains region (Sandberg et al., 1975; Turner and Otto, were recycled through underlying rocks of the Pioneer thrust plate or if 1988, 1995). Although the Milligen Formation likely composed part of they were ultimately sourced from the convergent margins of northern or the Roberts Mountain allochthon in east-central Idaho, the Pioneer thrust eastern North America (Link et al., 2014). is a Cretaceous structure and does not mark the trace of a Late Devonian– Mississippian fault system (Dover, 1980; Rodgers et al., 1995). METHODS AND MATERIALS Mississippian Copper Basin Group and equivalent rocks of the Cop- per Basin thrust plate (Figs. 2A, 2B) represent the Antler foreland basin Twelve rock samples from the Pioneer, Copper Basin, and Hawley sequence in east-central Idaho. Lower Mississippian flysch strata in the Creek thrust plates were collected for detrital zircon U-Pb geochronol- Pioneer Mountains comprise >4200 m of east- and north-prograding fan ogy (see locations in Fig. 2A). The suite includes three samples of the delta to submarine fan deposits that were rapidly buried (Wilson et al., Kinnikinic Quartzite (09LR01, 05TA09, 09TD10), one sample of the 1994; Link et al., 1996). Flexural loading tied to the emplacement of the Basin Gulch Quartzite Member of the Phi Kappa Formation (06PL13), Roberts Mountain allochthon and syndepositional normal faulting within two samples of the Milligen Formation (11LB04, 02TD10), one sample the foreland drove early subsidence within the narrow (~70 km wide) of the Jefferson Formation (05PL13), and five samples of the Copper Copper Basin depocenter (Wilson et al., 1994). Decompacted sedimen- Basin Group (09LB04, 05PL15, 40JMP94, 10JMP94) and equivalent tation rates for lower Tournaisian strata are ~950–1400 m/m.y. (Link et Salmon River assemblage (24PL09). Detrital zircons were separated using al., 1996), greater than most flexural troughs, but consistent with hybrid, conventional rock crushing, grinding, wet shaking table, and heavy liq- flexural- and fault-controlled basins (e.g., Houseknecht, 1986). Middle to uid and magnetic separation techniques. Three of the samples (09LR01, Upper Mississippian molasse strata consist of deltaic and shallow-marine 40JMP94, 10JMP94) were analyzed by secondary ion mass spectrometry siliciclastic rocks that are >1700 m thick and record waning sediment using a SHRIMP (sensitive high-resolution ion microprobe) instrument supply and accommodation space after a period of late Tournaisian uplift at the Australian National University following the methods of Williams and tilting (Link et al., 1996). (1998) and Link et al. (2005). The remaining nine samples were ana- Wilson et al. (1994) and Link et al. (1996) concluded that a transcur- lyzed by laser ablation–inductively coupled plasma–mass spectrometry rent plate setting best fit the evidence for both rapid subsidence and syn- (LA-ICP-MS) at the Arizona LaserChron Center, University of Arizona, depositional normal faulting in the Copper Basin depocenter. Following using the methods described by Gehrels et al. (2008). Analytical results, a model for Devonian–Mississippian transcurrent faulting from Arctic sample locations, and notes about data treatment are provided in Tables Canada to the southwestern United States proposed by Eisbacher (1983) DR1 and DR2 in the GSA Data Repository1. The U-Pb age results are that included field evidence for left-lateral shearing along the cratonic presented in relative probability plots with stacked histograms (Figs. 3–5) margin of the northern Canadian Cordillera, it was predicted (Wilson et made with the Isoplot Excel macro of Ludwig (2003). The modes for each al., 1994; Link et al., 1996) that the Copper Basin depocenter formed detrital zircon sample, which we informally report as probability age within a sinistral fault system. In this model, the Copper Basin Group peaks (e.g., Stewart et al., 2001; Dickinson and Gehrels, 2003; Gehrels, accumulated within a releasing bend basin that was bordered on its south 2012), were calculated with the AgePick Excel macro developed at the side by an uplifted restraining bend of Kinnikinic Quartzite near the Arizona LaserChron Center. Snake River Plain. For example, the conglomeratic Scorpion Mountain Dated zircons of four samples (11LB04, Milligen Formation, this Member of the Argosy Creek Formation, making up a submarine fan study; 4TD10, 01PL12, 3PL12, Sun Valley Group, Link et al., 2014) were with northward paleocurrents in the middle of the Copper Basin Group, analyzed for Hf isotope geochemistry at the Arizona LaserChron Center contains white clasts of Kinnikinic Quartzite that coarsen to boulder sized using laser routines, data reduction protocols, and interference corrections toward the south. Detrital zircon data reported here show that zircons in described by Gehrels and Pecha (2014). Analytical results and sample a quartzite cobble (sample 40JMP94) are identical to those in the Copper Basin Group quartz sandstone matrix (sample 10JMP94). Preacher et al. 1 (1995) recognized that these Tournaisian strata contained detrital zircons GSA Data Repository Item 2016277, Table DR1: SIMS detrital zircon U-Pb isotopic data and age results; Table DR2: LA-ICP-MS detrital zircon U-Pb isotopic data and older than 1800 Ma that were identical to those of the Valmy Forma- age results; Table DR3: LA-ICP-MS detrital zircon Hf isotope data, is available at tion in Nevada. Elsewhere in the Copper Basin Group, Mississippian www.geosociety.org/pubs /ft2016.htm, or on request from [email protected].

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35 Phi Kappa Fm. 30 D Sample 06PL13 LA-ICP-MS 25 n = 95/100 20 Number 15

18 Kinnikinic Quartzite Je erson Formation 12 16 C Sample 09LR01 C Sample 05PL13 SIMS LA-ICP-MS 14 10 n = 52/70 n = 92/100 12 8 10 Number 8 Number 6 6 4 4 2 2

25 Kinnikinic Quartzite 10 Milligen Formation B Sample 09TD10 B Independence ss. 20 LA-ICP-MS 8 Sample 11LB04 n = 97/100 LA-ICP-MS n = 69/100 15 6 Number Numbe r 10 4

5 2

30 Kinnikinic Quartzite 30 Milligen Formation 25 A Sample 5TA09 A Cait quartzite LA-ICP-MS 25 Sample 02TD10 20 n = 84/98 LA-ICP-MS 20 n = 72/75 15 15 Numbe r Numbe r 10 10

5 5

0 0.5 1.0 1.5 2.02.5 3.0 3.5 0 0.5 1.0 1.5 2.0 2.5 3.0 3.5 Age (Ga) Age (Ga) Figure 3. Probability density distribution stacked histo- Figure 4. Probability density distribution stacked histogram plots of Ordovician detrital zircon samples from gram plots of Devonian detrital zircon samples from the the Pioneer Mountains region, east-central Idaho. LA-ICP- Pioneer Mountains region, east-central Idaho. LA-ICP- MS—laser ablation–inductively coupled plasma–mass MS—laser ablation–inductively coupled plasma–mass spectrometry; SIMS—secondary ion mass spectrometry. spectrometry. (A) Emsian Cait quartzite quartz arenite (A) Kinnikinic Quartzite quartz arenite (sample 5TA09; of the lower Milligen Formation (sample 02TD10; East East Fork of Salmon River). (B) Kinnikinic Quartzite quartz Fork of Wood River). (B) Frasnian Independence sand- arenite (sample 09TD10; head of East Fork of Wood River). stone sublithic arenite of the upper Milligen Formation (C) Kinnikinic Quartzite quartz arenite (sample 09LR01; (sample 11LB04; east of Picabo). (C) Famennian Jef- west of Borah Peak, Lost River Range). (D) Phi Kappa ferson Formation sandstone (sample 05PL13; west of Formation, Basin Gulch Quartzite Member quartz arenite Borah Peak, head of Rock Creek, Lost River Range). (sample 06PL13; Little Fall Creek).

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Figure 5. Probability density distribution stacked histogram plots of Mis- Salmon River sissippian detrital zircon samples from the Pioneer Mountains region, 25 E assemblage east-central Idaho. LA-ICP-MS—laser ablation–inductively coupled plasma– Sample 24PL09 mass spectrometry; SIMS—secondary ion mass spectrometry. (A) Copper 20 LA-ICP-MS Basin Group lithic arenite (sample 09LB04; Little Copper Formation, Trail n = 89/100 Creek Road, east of Park Creek campground). (B) Copper Basin Group 15 lithic arenite (sample 05PL15; Argosy Creek Formation, Little Fall Creek). (C) Copper Basin Group quartz arenite clast (sample 40JMP94; Argosy Number 10 Creek Formation, Scorpion Mountain Member, near Argosy Peak). (D) Cop- per Basin Group quartz arenite close to 40JMP94 (sample 10JMP94; Argosy Creek Formation, Scorpion Mountain Member, near Argosy Peak). 5 (E) Salmon River assemblage sandstone (sample 24PL09; Thompson Creek molybdenum mine).

12 Copper Basin Gp. D Argosy Ck. Fm. 10 Sample 10JMP94 SIMS locations are provided in Table DR3. Initial 176Hf/177Hf ratios are reported 8 n = 41/53 as eHf(t) and represent the isotopic composition at the time of crystalliza- 6 tion relative to the chondritic uniform reservoir (Fig. 6). Number 4 RESULTS

2 Ordovician Kinnikinic Quartzite

Three samples of medium- to coarse-grained quartz arenite from the 12 Copper Basin Gp. Lost River Range (09LR01), Pioneer Mountains (09TD10), and along C Argosy Ck. Fm. the Salmon River near Bayhorse (05TA09) contain clear to pink to red 10 Sample 40JMP94 detrital zircons that range in size from 50 to 100 mm. The samples are SIMS dominantly composed of Paleoproterozoic (76%–88%) detrital zircons 8 n = 41/48 with probability age peaks that range from 1862 to 1828, 1959 to 1918, and 6 2099 to 2072 Ma (Figs. 3A–3C). Archean (3262–2500 Ma) detrital zircons

Number are found in all rock samples (9%–19%), whereas late Mesoproterozoic 4 (1072–1043 Ma) detrital zircons are only recognized in sample 09TD10. 2 Ordovician Phi Kappa Formation

A sample of fine-grained quartz arenite near the formation base (Basin 25 Copper Basin Gp. Gulch Quartzite Member) in the Pioneer Mountains (06PL13) contains B Argosy Ck. Fm. clear to pink to red detrital zircons that range in size from 25 to 50 m. The Sample 05PL15 m 20 LA-ICP-MS sample mostly yields Paleoproterozoic (81%) detrital zircons with prob- n = 105/105 ability age peaks of 1846, 1924, and 2079 Ma (Fig. 3D). Archean detrital 15 zircons compose 18% of the sample. Numbe r 10 Devonian Milligen Formation

5 A sample of coarse-grained quartz arenite from the Lower Devonian (Emsian) Cait quartzite (02TD10) has well-rounded, clear to pink detrital zircons that appear similar to those within Ordovician strata of the Pioneer Mountains area. The sample is mostly composed of Paleoproterozoic 12 Copper Basin Gp. A Little Copper Fm. (80%) detrital zircons with probability age peaks of 1839, 1922, and 10 Sample 09LB04 2082 Ma (Fig. 4A). Archean detrital zircons compose 19% of the sample. LA-ICP-MS A sample of medium-grained sublithic arenite from the Upper Devonian 8 n = 49/59 (Frasnian) Independence sandstone (11LB04) contains equant to elongate detrital zircons that are 30–100 mm. The sample is mainly composed of

Numbe r 6 Mesoproterozoic to latest Paleoproterozoic detrital zircons (71%) with prob- 4 ability age peaks of 1662 Ma and 1745 Ma (Fig. 4B). Smaller age groupings of early Paleozoic (450–428 Ma), early Neoproterozoic (954–928 Ma), and 2 Archean (2754–2508 Ma) detrital zircons are also present. Three Silurian detrital zircons in the Independence sandstone sample were analyzed for 0 0.5 1.0 1.5 2.0 2.5 3.0 3.5 Hf isotope geochemistry. Detrital zircons with ages of 428, 432, and 434 Age (Ga) Ma yielded eHf(t) values of -27.3, -5.6, and -10.7, respectively (Fig. 6).

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Depleted Mantle Pennsylvanian-Permian 15 Sun Valley Group Figure 6. An e versus U-Pb age diagram for detri- 1.0 Ga Hf(t) 10 01PL12 tal zircons from the Devonian Milligen Formation 04TD10 (11LB04) and Pennsylvanian–Permian Sun Valley 5 Group (01PL12, 4TD10, 03PL12) compared to ref- CHUR 1.5 Ga 03PL12 erence frames for the Pennsylvanian (Penn.) and 0 Late Devonian Triassic Cordilleran margin of southern British -5 Milligen Formation 2.0 Ga Independence sandstone Columbia (B.C.; Gehrels and Pecha, 2014), Ellesme- Hf(t) -10 11LB04 rian clastic wedge (Anfinson et al., 2012b; Gehrels ε and Pecha, 2014), and southern Appalachians (Muel- -15 2.5 Ga Penn. - Triassic ler et al., 2008). The eHf(t) values were calculated using -20 B.C. Cordillera the 176Lu decay constant of Scherer et al. (2001) and Söderlund et al. (2004) and the chondritic values of -25 3.0 Ga Ellesmerian clastic wedge Bouvier et al. (2008). The depleted mantle Hf evolu- -30 tion curves were calculated from values reported by Southern -35 Vervoort and Blichert-Toft (1999). Crustal evolution Appalachians lines from 1.0 to 3.0 Ga are plotted using 176Lu/177Hf 0 100 200 300 400 500 600 700 800 900 1000 = 0.015 (Goodge and Vervoort, 2006). CHUR—chondritic uniform reservoir. Age (Ma)

Devonian Jefferson Formation eHf(t) values of -16 to -4.5. A sample of Upper Pennsylvanian to lower Permian turbiditic sandstone (04TD10, Eagle Creek Member, Wood River A sample of Upper Devonian (Famennian) sandstone from the Jeffer- Formation, n = 8) contains Devonian (396 Ma), Silurian (434–421 Ma),

son Formation in the Lost River Range (05PL13) contains detrital zircons and Ordovician (448 Ma) detrital zircons with eHf(t) values of –32 to -5.5. that are 50–100 mm. The sample has an abundance of Mesoproterozoic A sample of lower Permian turbiditic sandstone (03PL12, Wilson Creek to late Paleoproterozoic detrital zircons (82%) that give probability age Member, Wood River Formation, n = 12) is mostly composed of Early peaks of 1652 Ma and 1848 Ma (Fig. 4C). Subsidiary probability age Devonian (419–413 Ma), Silurian (429 Ma), Ordovician (465 Ma), Cam- peaks occur ca. 505, 1145, 1304, 1386, 1568, and 2089 Ma. brian (501, 495 Ma) and Ediacaran (585, 557 Ma) detrital zircons with

negative eHf(t) values of -14 to -1; this sample also contains Pennsylva-

Mississippian Copper Basin Group and Salmon River Assemblage nian grains of 321 Ma and 308 Ma that yield eHf(t) values of -5.4 and +4.6, respectively. Four samples of the Copper Basin Group (09LB04, 05PL15, 40JMP94, 10JMP94) and one sample of the correlative Salmon River assemblage DISCUSSION (24PL09) in the Pioneer Mountains region contain clear to pink, sub- rounded to rounded detrital zircons that are 20–100 mm. Sedimentary Early Paleozoic Passive Margin System of Western Laurentia lithic sandstones from the basal Copper Basin Group (09LB04, Little Cop- per Formation) and overlying strata (05PL15, Argosy Creek Formation) Modern and ancient passive margin systems are characterized by well- have significant amounts of Paleoproterozoic (77%–82%) and Archean mixed siliciclastic strata (Ingersoll, 1990; Ingersoll et al., 1993) with detri- (18%–23%) detrital zircons and yield probability age peaks that range tal zircon ages that are much older than the time of sediment accumula- from 1783 to 1768, 1845 to 1808, 1978 to 1920, and 2055 to 2018 Ma tion (e.g., Cawood and Nemchin, 2001; Cawood et al., 2012). In western (Figs. 5A, 5B). Sample 40JMP94 is a cobble-sized clast of quartz arenite North America, such relationships are best preserved by lower Paleozoic in the Copper Basin Group (Scorpion Mountain Member, Argosy Creek sandstone units that crop out along the length of the Rocky Mountains and Formation) and sample 10JMP94 represents quartz sandstone matrix equivalent ranges from northern Canada to the southwestern United States stratigraphically near the clast. Both samples are dominated by Paleopro- (e.g., Gehrels and Ross, 1998; Gehrels et al., 2000a; Gehrels and Pecha, terozoic detrital zircons (92%) with most ages around 1868–1830 Ma and 2014). New sediment provenance results of Ordovician to Lower Devonian 2093 Ma (Figs. 5C, 5D). The Salmon River assemblage sample (20PL09) rocks in east-central Idaho strengthen this hypothesis and demonstrate contains abundant Paleoproterozoic detrital zircons (80%) and displays that the youngest detrital zircons in the Kinnikinic Quartzite, Phi Kappa probability age peaks of 1843 Ma and 2079 Ma (Fig. 5E). Formation, and lower Milligen Formation (Cait quartzite) are ~500–1300 m.y. older than the inferred depositional ages of their host rocks. The Pennsylvanian–Permian Sun Valley Group abundance of Paleoproterozoic and Archean detrital zircons in Ordovi- cian to Lower Devonian strata of east-central Idaho (Fig. 7A; this study), Link et al. (2014) reported the detrital zircon U-Pb signatures of Sun Great Basin of Nevada (Fig. 7B), and southern British Columbia (Fig. 7C) Valley Group strata in the Pioneer Mountains. We analyzed 35 zircons therefore supports the presence of an established Cordilleran passive mar- from 3 samples studied by Link et al. (2014) for Hf isotope geochemistry gin system that was the site of long-term sediment recycling (e.g., Ketner, (see locations in Fig. 2; results in Fig. 6). A sample of Middle Pennsyl- 1968; Cawood et al., 2012). Despite the evidence for episodic rifting and vanian shallow-marine sandstone (01PL12, Hailey Member, Wood River magmatism in western Canada and United States (e.g., Cecile et al., 1997; Formation, n = 15) has Devonian (393 and 379 Ma), Silurian (431 and Lund et al., 2010), early Paleozoic zircons are only locally preserved in 426 Ma) and Ediacaran to Cryogenian (664–588 Ma) detrital zircons that the Cambrian–Devonian sedimentary record (e.g., Todt and Link, 2013;

yield positive eHf(t) values of +4 to +14, whereas some other Ordovician Gehrels and Pecha, 2014). The detrital zircon signatures of Ordovician to Silurian to grains (470, 444, 436 Ma) are characterized by negative to Lower Devonian passive margin strata in east-central Idaho instead

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Frasnian strata of the Independence sandstone are part of a regional sub- East-central Idaho (this study) A Ordovician-Devonian strata marine fan succession that presumably sampled rocks to the west of Mil- 5 samples, n = 400 ligen depocenter (Link et al., 1995). Despite its provenance signature being significantly different from that of the lower Milligen Formation (Cait quartzite), the youngest detrital zircons in the Independence sand- Great Basin, Nevada stone sample are mid-Silurian (ca. 430 Ma) and predate the depositional B Ordovician strata age of the unit by ~50 m.y. This sample consists of well-mixed turbiditic 2 samples, n = 312 sandstone and therefore suggests that an adjacent Devonian magmatic arc complex, if present, did not generate abundant zircon, or that such arc-type rocks were not sampled by this part of the submarine fan system. Southern British Columbia Three potential source regions are considered in the following (western, Ordovician strata northern, and eastern Laurentian margins) to evaluate mid-Paleozoic prov- C 1 sample, n = 193 enance ties with Upper Devonian strata (Fig. 8A) of east-central Idaho.

Potential Sources from the Western Laurentian Margin Ellesmere Is. and N. Greenland The North American Cordillera contains linear belts of subduction- Proterozoic-Cambrian strata D 16 samples, n = 972 related rocks, syntectonic strata, and volcanic- and sediment-hosted sulfide occurrences that provide compelling evidence for a west-facing, mid- Paleozoic convergent margin system to have existed along western Lau- rentia (e.g., Albers and Bain, 1985; Richards, 1989; Rubin et al., 1990; Western Newfoundland Proterozoic-Ordovician strata Mortensen, 1992; Erdmer et al., 1998; Nelson et al., 2002, 2006; Piercey E 6 samples, n = 341 et al., 2004, 2006; Devine et al., 2006; Dusel-Bacon et al., 2006; Paradis et al., 2006; Ruks et al., 2006). Field-based studies in western Canada have further recognized mid-Paleozoic deformation and metamorphism 0 0.5 1.0 1.5 2.0 2.53.0 3.54.0 within continental margin rocks of known or inferred Laurentian crustal Age (Ga) affinity (e.g., Klepacki and Wheeler, 1985; Root, 2001; Colpron et al., 2006; Berman et al., 2007; Kraft, 2013). In the northern U.S. Rocky Figure 7. Detrital zircon reference frames for Laurentian passive margin Mountains, the record of Devonian convergent margin activity is typi- strata of western United States, Canada, and Greenland. (A) Ordovician to Lower Devonian strata (Kinnikinic Quartzite, Phi Kappa Formation, Cait cally obscured by Mesozoic tectonism and arc magmatism. For example, quartzite of lower Milligen Formation), Pioneer Mountains, east-central Paleozoic rocks in the Pioneer thrust plate, including deformed Milligen Idaho (this study). (B) Ordovician strata (Valmy Formation, Eureka Quartz- Formation strata, were telescoped during the Sevier orogeny, intruded by ite), Great Basin, Nevada (Gehrels and Pecha, 2014). (C) Ordovician strata the regionally extensive Idaho batholith, and overlain by Eocene volcanic (Mount Wilson Formation), British Columbia, Canada (Gehrels and Ross, units (Rodgers et al., 1995; Gaschnig et al., 2010, 2011, 2013). 1998; Gehrels and Pecha, 2014). (D) Proterozoic to Cambrian strata (Grant The Eastern Klamath and Northern Sierra terranes are largely under- Land Formation, Nesmith beds, Portfjeld Formation, Morænso Formation, Inuiteq Sø Group), northern Greenland (Kirkland et al., 2009) and Elles- lain by early to mid-Paleozoic convergent margin rocks and have long mere Island, Canada (Beranek et al., 2013b). (E) Proterozoic to Ordovician been considered potential candidates for the so-called Antler arc in the strata (Blow-Me-Down Brook, American Tickle, Summerside, Hawke Bay, western United States (e.g., Nilsen and Stewart, 1980; Schweickert and South Brook, and Bradore Formations), western Newfoundland (Cawood Snyder, 1981; Poole et al., 1992; Gehrels et al., 2000b). Lindsley-Griffin and Nemchin, 2001). et al. (2006, 2008) provided the most recent overview of these terranes. Grove et al. (2008) reported that Lower to Middle Devonian strata of the Eastern Klamath terrane in northern California yield unimodal 480–380 reflect provenance from Precambrian (ca. 1850, 1920, 2080, and 2700 Ma or 490–410 Ma detrital zircon populations (Sissel Gulch Graywacke Ma) crystalline basement units and their supracrustal derivatives. The new and Gazelle Formation) or mixed 480–410 Ma and 2000–1000 Ma age U-Pb results from the Pioneer Mountains are most consistent with Pre- signatures (Duzel Phyllite and Moffett Creek Formation) with probability cambrian sources of the northwestern Canadian shield (e.g., Slave, Hottah, peaks of ca. 1000, 1450, and 1650 Ma (Figs. 8B, 8C). These detrital zircon Great Bear, Fort Simpson, and Trans-Hudson basement domains; Hoff- ages support local provenance from rock units in the Klamath Mountains man, 1988; Hanmer et al., 2004), including unique-aged Paleoproterozoic (Yreka and Trinity subterranes), including 435–400 Ma plutonic rocks, (2100–2000 Ma) rocks of the Buffalo Head and Chinchaga terranes in Devonian volcanic and volcaniclastic rocks, and cratonal strata that were the Peace River Arch region that are diagnostic of northwest Laurentian metamorphosed to blueschist facies (e.g., Wallin et al., 1995; Wallin and provenance (e.g., Gehrels and Ross, 1998; Gehrels and Pecha, 2014). Metcalf, 1998; Grove et al., 2008; Lindsley-Griffin et al., 2008). Metasedi- mentary rock units of the Northern Sierra terrane in northern California Devonian Provenance Trends: A Record of the Passive to Active- (Sierra City mélange, Shoo Fly Complex) that are intruded by the 372 Margin Transition? ± 6 Ma Bowman Lake batholith (Cecil et al., 2012) have detrital zircon age distributions similar to those of Eastern Klamath terrane strata (Figs. Convergent margin basins typically have first- or second-cycle detrital 8D, 8E; Grove et al., 2008) and likely have provenance from mid-Silurian zircons that closely approximate the age of deposition (e.g., Cawood et al., and Ediacaran igneous rocks (Saleeby et al., 1987; Saleeby, 1990) and 2012). The geology of the upper Milligen Formation is broadly suggestive variably deformed cratonal strata (Harding et al., 2000). of such an active plate setting, including evidence for mafic volcanism and Devonian strata of the Chase formation compose part of the enigmatic localized faulting, and therefore provides a unique opportunity to inves- basement to southern Quesnellia (Okanagan subterrane) in the Okanagan- tigate mid-Paleozoic tectonism in the northern U.S. Rocky Mountains. Kootenay region of southeastern British Columbia (Fig. 1; Monger et

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near the British Columbia–Alberta border, Late Devonian ties with an East-central Idaho (this study) A U. Milligen & Je erson Fms. outboard source are further demonstrated by west-derived continental 2 samples, n = 161 margin strata of the Sassenach Formation (Savoy et al., 2000; Stevenson et al., 2000) that yield Archean to early Paleozoic detrital zircons (Geh- rels and Pecha, 2014) with age peaks of ca. 440, 1220, 1430, 1630, and Eastern Klamath terrane, CA 1720 Ma (Fig. 8G). In combination with evidence for Middle Devonian B Duzel Phyl. & Mo ett Ck. Fm. deformation in the adjacent Purcell Mountains of southeastern British 8 samples, n = 246 Columbia (Fig. 1; Root, 2001), it seems likely that the Okanagan subterrane was juxtaposed with the distal Cordilleran margin by Late Devonian time (Colpron and Nelson, 2009; Kraft, 2013). Eastern Klamath terrane, CA Detrital zircon U-Pb and Hf isotope results of the present study support C Sissel Gulch Gr. & Gazelle Fm. the hypothesis that some Upper Devonian strata of the Pioneer Mountains 2 samples, n = 182 were derived from the erosion of a Paleozoic arc built on Proterozoic crust. We propose that convergent margin rocks of the Eastern Klamath, Northern Sierra, and Quesnellia terranes were western source areas for the Indepen- Northern Sierra terrane, CA dence sandstone and Jefferson Formation of east-central Idaho, and more D Sierra City mélange, Shoo Fly 1 sample, n = 99 broadly, the Sassenach Formation in the southern Canadian Rocky Moun- tains. Future studies are therefore predicted to identify evolved zircon Hf isotope signatures for Eastern Klamath, Northern Sierra, and Quesnellia arc-type rocks and arc-proximal strata. For example, the Independence Northern Sierra terrane, CA Sierra City mélange, Shoo Fly sandstone contains 434–428 Ma detrital zircons (Fig. 6) with evolved Hf E 1 sample, n = 54 isotopic compositions [eHf(t) = -27.3 to -5.6; X = -14.5] and Archean to Proterozoic model ages (2700–1530 Ma). Most similar-aged (444–426 Ma; n = 5/7, 71%) detrital zircons in the basal Sun Valley Group (01PL12; Middle Pennsylvanian Hailey Member, Wood River Formation), a unit that Quesnellia, British Columbia Chase formation Link et al. (2014) suggested may have recycled parts of the underlying F 4 samples, n = 87 Milligen Formation, yield eHf(t) < 0 and Paleoproterozoic to Mesoprotero- zoic model ages that are comparable with the Independence sandstone results. Upper Pennsylvanian to lower Permian strata of the Eagle Creek (04TD10) and Wilson Creek (03PL12) Members are similarly dominated Cordilleran margin, B.C. by 448–413 Ma zircons with evolved values of 32 to 1 (n = 11/11, G Sassenach Formation eHf(t) - - 1 sample, n = 100 100%), but Link et al. (2014) concluded that these Sun Valley Group strata have eastern or northern provenance from arc rocks of the Ellesmerian, Appalachian, or Caledonian orogenic belts. Pennsylvanian (Spray Lakes 0 0.5 1.0 1.5 2.0 2.5 3.0 3.5 4.0 Group) and Triassic (Whitehorse Formation) marine strata in the British Age (Ga) Columbia Cordillera show detrital zircon U-Pb age and Hf isotope signa- Figure 8. Detrital zircon reference frames for Devonian convergent margin tures that compare favorably with those of the Independence sandstone and strata of western United States and Canada. B.C.—British Columbia; CA— Sun Valley Group (Fig. 6; Gehrels and Pecha, 2014), which suggests that California, Gr.—graywacke; Fms.—formations; Phyl.—phyllite; Cr.—Creek; Paleozoic orogenic activity, regardless of its location around the edges of U.—Upper. (A) Independence sandstone of the upper Milligen Formation Laurentia, led to fundamental changes in the isotopic composition of the (Late Devonian) and Jefferson Formation (Late Devonian), Pioneer Moun- post-Devonian Cordilleran margin (e.g., Boghossian et al., 1996). tains (this study). (B) Duzel Phyllite and Moffett Creek Formation (Early Devonian) (Grove et al., 2008). (C) Sissel Gulch Graywacke and Gazelle Potential Sources from the Northern Laurentian Margin Formation (Early to Middle Devonian) (Grove et al., 2008). (D) Sierra City mélange (pre-Late Devonian) (Grove et al., 2008). (E) Sierra City mélange Upper Devonian strata of the Milligen and Jefferson Formations (pre–Late Devonian) (Grove et al., 2008). (F) Chase formation (Middle to Late together record an influx of ca. 450–430 Ma and 1650–930 Ma detrital Devonian) (Lemieux et al., 2007). (G) Sassenach Formation (Late Devonian) zircons into the Cordilleran margin system, with only minor evidence (Gehrels and Pecha, 2014). for the 2700–1800 Ma age populations that were dominant in Lower Devonian and older passive margin strata (Fig. 8A). An analogous provenance change is revealed by Silurian and Devonian–Mississippian rocks al., 1991) and may represent a portion of the Antler orogenic system in that document the incursion of 450–430 Ma, 1650–930 Ma, and other southern Canada (Colpron and Nelson, 2009). Chase formation rocks detrital zircons along the northern Laurentian or Franklinian margin (e.g., yield Archean to early Paleozoic detrital zircons (Lemieux et al., 2007) Gehrels et al., 1999; Beranek et al., 2010, 2015; Lemieux et al., 2011). with primary age peaks of ca. 410, 1530, 1700, and 1850 Ma (Fig. 8F). These early Paleozoic and Proterozoic detrital zircons were shed from the Although Silurian–Early Devonian magmatic rocks are not yet recognized south-vergent, Ellesmerian orogenic belt in Late Devonian–Mississippian in the Okanagan-Kootenay region, mid-Paleozoic conglomeratic strata time, carried southwest by terrestrial and marine transport systems, and assigned to the distal North American margin succession near Kootenay eventually deposited into the Cordilleran shallow-water shelf (Ross et al., Lake (Milford group), <100 km east of Quesnellia, contain ca. 418 and 1997; Beranek et al., 2010). It has been proposed that Ellesmerian fore- 431 Ma granitoid boulders (Roback et al., 1994) with an inferred western land basin detrital zircons mark the erosion of accreted arcs with Baltican source from an uplifted block called the Okanagan high (e.g., Thompson or northern Caledonian crustal affinities along northern North America et al., 2006; Colpron and Nelson, 2009). In the southern Canadian Rockies (Beranek et al., 2010, 2015; Lemieux et al., 2011; Anfinson et al., 2012a,

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2012b, 2013, 2016). An Ellesmerian provenance for Frasnian–Famennian Several models have been proposed to explain the driving forces strata in east-central Idaho is therefore permissive, but it calls for detrital responsible for Mississippian subsidence and syntectonic sedimentation zircons to be transported >3000 km from their sites of origin during the adjacent to the Roberts Mountain allochthon (e.g., Speed and Sleep, 1982; Late Devonian. The Independence sandstone sample, however, yields Trexler and Nitchman, 1990; Dorobek et al., 1991; Miller et al., 1992;

434–428 Ma detrital zircons with evolved Hf isotopic compositions [eHf(t) Trexler et al., 2003). Because one can identify in syntectonic strata the = -27.3 to -5.6; X = -14.5] and Hf model ages (2700–1530 Ma) that are geological elements that supply clastic detritus to foreland basins, the not typical of such Ellesmerian strata (Fig. 6). For example, 470–400 Ma provenance signatures of Mississippian flysch deposits in east-central detrital zircons in Upper Devonian strata of eastern Alaska (Nation River Idaho give new insights into the Antler orogenic system. In the Pioneer Formation) and the Canadian Arctic Islands (Blackley and Parry Islands Mountains, Lower Mississippian syntectonic strata were south and west

Formations) yield more juvenile eHf(t) values that range from -2 to +8 derived (Wilson et al., 1994) and mostly contain recycled Archean to (X = +3.5; Anfinson et al., 2012b) and +1 to +15 (X = 8.2; Gehrels and Paleoproterozoic detrital zircons and lithic fragments that imply prov- Pecha, 2014), respectively. enance from Roberts Mountain allochthon units in the Antler highlands (Phi Kappa and Milligen Formations) and underlying Ordovician pas- Potential Sources from the Eastern Laurentian Margin sive margin rocks of the Copper Basin and Hawley Creek thrust plates Some studies have argued for the incursion of Paleozoic and Meso- (Fig. 9A). These data are consistent with Antler flysch in the Pioneer proterozoic detrital zircons into Cordilleran basins to indicate provenance Mountains being partially derived from intraforeland blocks of Kinniki- from the Appalachian orogen of eastern Laurentia (e.g., Dickinson and nic Quartzite that were uplifted during regional tectonism (Wilson et al., Gehrels, 2003; Gehrels et al., 2011; Link et al., 2014; Lawton et al., 2015). 1994; Link et al., 1996). At a broader scale, recycled Archean to Paleo- For example, a central Appalachian provenance is interpreted for upper proterozoic detrital zircons of Laurentian affinity also dominate Middle Paleozoic sandstones of the Grand Canyon that are dominantly composed to Upper Mississippian foredeep strata (Tonka Formation) in the Great of ca. 475–270 Ma and 1200–1000 Ma detrital zircons (Gehrels et al., Basin of Nevada (Fig. 9B); however, rare syndepositional (340 ± 8 Ma, 2011). Scenarios for eastern Laurentian provenance generally invoke 346 ± 4 Ma) contributions to this unit (Gehrels and Pecha, 2014) imply pan-continental river systems to transport Appalachian detritus to Cordil- proximity to an outboard arc system. Lower Mississippian strata of the leran basins. Most of the early Paleozoic arc terranes in the Appalachians Antler backbulge basin in the Great Basin of southwestern Utah (Joana formed along the margins of Gondwana by the recycling of Mesoprotero- Limestone) have provenance connections with both east-central Idaho and zoic and older crust (e.g., Nance et al., 2008). Early Paleozoic detrital Nevada flysch successions and are characterized by recycled Archean and zircons that are derived from Gondwanan source rocks therefore yield Paleoproterozoic detrital zircons (Fig. 9C) with only minor evidence of

moderate to evolved eHf(t) values of +5 to -15 (e.g., Mueller et al., 2008; Ediacaran to early Paleozoic components (Cole et al., 2015). Bahlburg et al., 2010, 2011; Reimann et al., 2010). Sediment recycling in the northern Cordillera took place within Although the available Hf isotope data for Gondwanan-affinity zir- restricted marine basins that were located behind a west-facing continental cons in the Appalachians (Mueller et al., 2008) broadly overlap with our Independence sandstone results (Fig. 6), an eastern Laurentian source for Upper Devonian strata is likely inconsistent with the western deriva- East-central Idaho (this study) tion of upper Milligen Formation turbidites. However, Eagle Creek and A Copper Basin Gp. & equiv. Wilson Creek strata of the Sun Valley Group, along with the correlative 5 samples, n = 325 Tensleep and Weber Sandstones in Wyoming, contain detrital zircon age populations that suggest that big rivers from the Appalachians supplied sediment to the northern U.S. Rocky Mountains by Late Pennsylvanian Great Basin, Nevada time (Link et al., 2014). As discussed here, the evolved e values of Tonka Formation Hf(t) B 1 sample, n = 105 Eagle Creek (04TD10) and Wilson Creek (03PL12) detrital zircons mostly agree with the southern Appalachian reference frame (Fig. 6). These and other data imply that the Transcontinental Arch, a long-lived positive feature of the central United States, prevented eastern Laurentian Great Basin, Utah Joana Limestone zircons from entering Late Devonian basins of the northern U.S. Rocky C 1 sample, n = 110 Mountains (Link et al., 2014).

Mississippian Sediment Recycling in the Antler Foreland Basin Cordilleran margin, Yukon Prevost Formation, Earn Group Foreland basins are filled with deep-water flysch or shallow-water D 1 sample, n = 74 molasse deposits that generally have a recycled orogen provenance from uplifted continental margin rocks (e.g., Dickinson et al., 1983b; Garzanti et al., 2007). Peripheral and retroarc foreland basins, such as those in 0 0.5 1.0 1.5 2.02.5 3.03.5 4.0 the Himalayan and Cordilleran orogens, respectively, are subsequently Age (Ga) dominated by detrital zircons that are older than the age of sediment accumulation, with only minor evidence for syndepositional magmatic Figure 9. Detrital zircon reference frames for Mississippian strata in western activity (e.g., Cawood et al., 2012). For example, Mesozoic foreland United States and Canada. (A) Copper Basin Group (Gp.) and equivalents basin deposits to the east of the Rocky Mountains fold and thrust belt of the Salmon River assemblage (Early Mississippian), Pioneer Mountains, east-central Idaho (this study). (B) Tonka Formation (Middle to Late Mis- were primarily sourced from uplifted passive margin strata and contain sissippian), Nevada (Gehrels and Pecha, 2014). (C) Joana Limestone (Early recycled Proterozoic and Archean detrital zircons of Laurentian affinity Mississippian), Utah (Cole et al., 2015). (D) Prevost Formation, Earn Group (e.g., Fuentes et al., 2009; Hadlari et al., 2014, 2015; Lawton et al., 2014). (Late Devonian–Early Mississippian), Yukon (Beranek et al., 2010).

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arc system (e.g., Nelson et al., 2006). In Yukon and northern British al., 1994; Wallin and Metcalf, 1998; Grove et al., 2008). Antler foreland Columbia, these restricted basins were filled by west- to southwest-derived basin rocks in the western United States, which in part were derived by turbidite successions and mafic to felsic volcanic rocks and locally contain the recycling of Roberts Mountain allochthon units, are similarly endowed sedimentary exhalative and volcanogenic massive sulfide occurrences in Paleoproterozoic and Archean detrital zircons with only minor con- that are indicative of extensional or transtensional backarc environments tributions from an inferred Mississippian arc (ca. 340 Ma; Gehrels and (Gordey et al., 1987; Gordey and Anderson, 1993; Piercey et al., 2004). Pecha, 2014). Despite the lack of robust evidence for the Roberts Moun- Upper Famennian to Tournaisian submarine fan complexes in eastern tain allochthon being part of an accretionary prism or subduction zone Yukon (Prevost Formation, Earn Group) are dominated by recycled complex (see review by Miller et al., 1992), detrital zircon provenance Archean and Paleoproterozoic detrital zircons (Fig. 9D; Beranek et al., data may provide a nonunique test of the arc-continent collisional model 2010), similar to those that characterize the Antler foreland basin in the (Gehrels et al., 2000b). western United States, and were most likely derived from uplifted blocks of lower Paleozoic passive margin strata (e.g., Gordey et al., 1987; Gordey Noncollisional Models and Anderson, 1993). Eisbacher (1983) proposed that mid-Paleozoic Most noncollisional models for the Antler orogeny feature craton- sedimentation, volcanism, and base-metal mineralization in the northern directed retroarc deformation in the region behind a west-facing con- Cordillera was the result of a sinistral-oblique fault system that connected tinental arc (e.g., Burchfiel and Davis, 1972; Miller et al., 1984, 1992). the Ellesmerian orogenic system of Arctic Canada with the Antler orog- The Roberts Mountain allochthon in these scenarios consists of outer eny in the southwestern United States. In northern Yukon and Northwest continental margin strata that accumulated in extensional or transten- Territories, Eisbacher (1983) based this hypothesis on evidence for the sional basins prior to Devonian subduction initiation along western North sinistral transcurrent displacement of Proterozoic rocks within the Rich- America. For example, lower Paleozoic alkaline volcanic rocks and syn- ardson-Hess fault zone. genetic sulfide mineralization in the Roberts Mountain allochthon and outer North American parautochthon are consistent with an extensional Implications for Models of the Antler Orogeny or transtensional tectonic setting (e.g., Turner and Otto, 1988; Miller et al., 1992; Otto and Zieg, 2003). Broadly analogous basinal environments The Late Devonian–Mississippian Antler orogeny is arguably the most are also suggested for the continental margin of western Canada (e.g., significant plate tectonic event in the early history of the North American Goodfellow et al., 1995; Cecile et al., 1997; Goodfellow and Lydon, 2007). Cordillera and culminated with the east-directed emplacement of the Roberts Mountain allochthon strata yield detrital zircon signatures that Roberts Mountain allochthon onto the adjacent continental margin (e.g., are compatible with western Laurentian provenance (Figs. 7A, 7B) and Roberts et al., 1958; Burchfiel and Davis, 1975; Nilsen and Stewart, 1980). therefore support the paleogeographic assumptions of the noncollisional Although the framework geology of this orogenic belt in the Great Basin model. Mississippian syntectonic strata of the Antler foreland in east- of Nevada has been studied for decades, there is still no consensus on central Idaho and Nevada contain recycled Precambrian detrital zircons the driving forces responsible for Antler tectonism. New detrital zircon that were sourced from uplifted passive margin rocks (Figs. 9A, 9B) results from the Pioneer Mountains of east-central Idaho, in combination and show only minor inputs from the adjacent arc, similar to Mesozoic with constraints from published studies, allow us to examine three plate foreland basin systems of western North America (Fuentes et al., 2009; tectonic scenarios proposed for the Antler orogeny. Raines et al., 2013). Burchfiel and Royden (1991) proposed a noncollisional model in Arc-Continent Collision Models which a generally west-facing arc system is subjected to an episode of Arc-continent collision models for the Antler orogeny propose that subduction along its inboard eastern side. This model was based on mod- Late Devonian–Mississippian deformation resulted from the west-facing ern Apennine-type orogenic belts in the Mediterranean that display the Cordilleran passive margin clogging the subduction zone of an east-facing foreland-directed migration of such retrograde subduction zones, likely arc system (Burchfiel and Davis, 1972; Schweickert and Snyder, 1981; driven by slab rollback, and extension in the overriding plate (Royden and Speed and Sleep, 1982; Dickinson, 2006). Roberts Mountain allochthon Burchfiel, 1989). The Roberts Mountain allochthon in this model would strata in these scenarios compose accretionary prism or subduction com- comprise accretionary prism rocks that were tectonically emplaced on plex rocks that were thrust eastward onto the Cordilleran platform as the the Cordilleran shelf as a result of the migrating arc system approaching arc approached the continent (Speed and Sleep, 1982; Dickinson et al., the continental margin. Burchfiel and Royden (1991) argued that such 1983a). The Northern Sierra and Eastern Klamath terranes may have arcs to do not truly collide, and that this type of passive accretion could composed part of the converging Antler arc; however, it is uncertain if explain the absence of a collided arc to the west of the Antler belt. As the timing of Early to Middle Devonian deformation and metamorphism discussed herein for the arc-continent collision model, the Precambrian- therein (e.g., Cashman, 1980; Saleeby et al., 1987; Wallin et al., 2000) is dominated detrital zircon signatures of most western assemblage units consistent with that required by models for Late Devonian–Mississippian may be inconsistent with the Roberts Mountain allochthon composing arc-continent collision and foreland basin sedimentation. Because accre- part of an accretionary prism. tionary prism and subduction complex rocks typically show evidence of syndepositional magmatic activity (e.g., Amato et al., 2013; Chapman et Oblique Convergence Models al., 2016), Roberts Mountain allochthon strata in this model are expected Recent models for the Antler orogeny predict that mid-Paleozoic Cor- to contain Paleozoic detrital zircons from the adjacent Sierra-Klamath dilleran orogenesis was linked to oblique convergence along western arc. The Precambrian-dominated detrital zircon signatures of most Rob- North America. Wright and Wyld (2006) proposed that a migrating sub- erts Mountain allochthon units appear to be inconsistent with Paleozoic duction system, analogous to that of the modern Scotia and Caribbean arc provenance; however, Upper Devonian Milligen Formation strata in arcs, transported the Alexander, Eastern Klamath, and Northern Sierra the Pioneer Mountains yield Silurian detrital zircons that broadly sup- terranes from the peri-Gondwanan realm around the southern margin of port ties with known rock assemblages of the Northern Sierra, Eastern Laurentia to the paleo–Pacific Ocean (eastern Panthalassa) during the early Klamath, and Quesnellia terranes (e.g., Saleeby et al., 1987; Roback et Paleozoic. In their model, subsequent mid-Paleozoic Antler tectonism in

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the Great Basin was the result of north-propagating, dextral-oblique con- and northern Greenland (Fig. 7D) and western Newfoundland (Fig. 7E) vergence and juxtaposition of these arc fragments against the Cordilleran yield Archean to Paleoproterozoic age peaks that compare favorably with margin. Wright and Wyld (2006) considered rock units of the Roberts Cordilleran margin samples. Passive margin rocks in areas such as western Mountain allochthon, except the Ordovician Vinini Formation, to have Newfoundland (Fig. 7E), however, are more proximal to the Grenville non–western Laurentian origins. orogen of eastern North America and therefore yield greater amounts late Colpron and Nelson (2009, 2011) modified this migrating subduc- Mesoproterozoic detrital zircons while lacking 2100–2000 Ma grains that tion system hypothesis and proposed that the basement domains of the are typical of Peace River Arch provenance. Eastern Klamath, Northern Sierra, and Quesnellia terranes evolved near northeastern Baltica and the northern Caledonian orogen prior to west- Middle to Late Devonian ward transport around the northern margin of Laurentia. According to Our preferred model for Middle to Late Devonian paleogeography Colpron and Nelson (2009), subsequent Middle to Late Devonian sub- generally follows the conclusions of Colpron and Nelson (2009) and duction initiation along western North America was broadly linked to a features a migrating subduction system near northwestern Canada (Fig. sinistral transcurrent fault system that nucleated near northwestern Canada 10B). In the Colpron and Nelson (2009) model, this migrating subduc- and propagated southward to the southwestern United States. Sinistral tion system transported exotic crustal fragments from the northern end of transcurrent faulting in this model led to the north to south, time-trans- the Caledonides westward into Panthalassa. A sinistral transcurrent fault gressive juxtaposition of the Baltican-Caledonian–affinity terranes against along the Cordilleran margin spawned from this migrating subduction the Cordilleran margin, which is in part evidenced by Middle Devonian system and accommodated the southward displacement of some exotic deformation in the Purcell Mountains of southeastern British Columbia crustal fragments, such as the basement units of the Eastern Klamath, and Late Devonian–Mississippian Antler tectonism in Idaho and Nevada. Northern Sierra, and Quesnellia terranes. Eifelian folding and thrusting Colpron and Nelson (2011) concluded that an average velocity of ~5 cm/yr in the Purcell Mountains of British Columbia (Root, 2001) likely records is required to accommodate the translation of exotic terranes from north- part of the oblique convergence associated with this fault system in southwestern Canada to the southwestern United States during the Devonian. eastern British Columbia (Fig. 10B) and is broadly consistent with the The accreted exotic blocks, along with existing parts of the Laurentian sinistral transcurrent hypothesis of Eisbacher (1983) for the Canadian continental margin (e.g., Yukon-Tanana; Colpron et al., 2007), formed Cordillera. Linde et al. (2016) proposed that some Ordovician rock units the substrate to a west-facing continental arc system that subsequently of the Roberts Mountain allochthon in Nevada originally formed near the underwent backarc rifting to generate a marginal ocean basin that we U.S.-Canadian border, north of the Great Basin, and were subsequently refer to as the Slide Mountain Ocean (e.g., Miller et al., 1984, 1992; translated southward by a Devonian sinistral fault. Mortensen, 1992; Creaser et al., 1997; Piercey et al., 2004; Nelson et al., A transcurrent plate setting is consistent with the geology of Middle 2006; Colpron et al., 2007). to Upper Devonian strata in the Pioneer Mountains. For example, the Milligen Formation records Middle to Late Devonian extension or trans- Paleozoic Paleogeography tension that was associated with mafic volcanism, localized extensional faulting, and exhalative base-metal mineralization (e.g., Turner and Otto, Paleogeographic scenarios for three time slices (Middle to Late Ordo- 1988; Link et al., 1995). The 450–430 Ma and 1650–930 Ma detrital vician, Middle to Late Devonian, and Late Devonian to Early Mississip- zircons observed in the Late Devonian Independence sandstone and Jef- pian) are discussed next and shown in Figure 10. ferson Formation (Fig. 8A) and Late Devonian Sassenach Formation in the southern Canadian Rockies (Fig. 8G) imply proximity to exotic rocks Middle to Late Ordovician of the Eastern Klamath, Northern Sierra, and Quesnellia terranes after The detrital zircon signatures of shallow-water shelf (e.g., Kinnikinic their oblique juxtaposition along the Cordilleran margin. Middle to Late Quartzite, Eureka Quartzite, Mount Wilson Formation) and deep-water Devonian provenance ties between the exotic terranes and the Cordil- slope and rise (e.g., Phi Kappa Formation, Valmy Formation) strata indi- leran margin broadly agree with average displacement rates of ~5 cm/yr cate shared provenance from ca. 1850, 1920, 2080, and 2700 Ma rocks from northwestern Canada to the southwestern United States (Colpron in northwestern Laurentia and argue for the Cordilleran margin to be the and Nelson, 2011). site of extensive sediment recycling during the Middle to Late Ordovi- cian. The north-facing Cordilleran margin straddled the paleoequator Late Devonian to Early Mississippian at this time, with longshore currents (Ketner, 1968), perhaps driven by A west-facing continental arc system was present along the Cordil- southwest-directed trade winds (northeasterlies), accommodating the leran margin in Late Devonian to Early Mississippian time (Fig. 10C). transport of quartz-rich sediment from the Peace River Arch to the south- East-dipping subduction probably initiated during the Middle to Late western United States (Fig. 10A). Middle to Late Ordovician sea-level Devonian and propagated southward from northwestern Canada to the fluctuations may have also influenced sediment provenance signatures on southwestern United States (Colpron and Nelson, 2009). Backarc exten- a regional scale. For example, the maximum exposure of cratonic rocks sion and opening of a marginal ocean basin in the region behind the arc in the U.S. Rocky Mountains occurred during an Ordovician lowstand, was subsequently ongoing in the northern Cordillera by the Early Missis- which in some cases resulted in provenance signatures being dominated sippian (e.g., Piercey et al., 2004) and also likely propagated from north by proximal sources instead of the Peace River Arch (Pope et al., 2008; to south (Fig. 10C). Baar, 2009; Wulf, 2011). Mississippian Copper Basin Group strata document rapid subsidence, Proterozoic to lower Paleozoic strata that characterize the Franklinian syndepositional faulting, and reworking of lower Paleozoic passive mar- and Appalachian passive margins of Laurentia (Fig. 10A) are similarly gin strata in the Antler foreland basin of east-central Idaho. We favor a endowed in Precambrian detrital zircons that are much older than the sinistral-oblique tectonic setting for the Copper Basin depocenter based time of sediment deposition; this supports the large-scale recycling of on the results of previous field (e.g., Wilson et al., 1994; Link et al., 1996) cratonal rocks after the breakup of supercontinent Rodinia (e.g., Hadlari and tectonic analysis (Eisbacher, 1983; Reid and Dorobek, 1991; Colpron et al., 2012; Beranek et al., 2013b). Detrital zircons from Ellesmere Island and Nelson, 2009, 2011) studies. Following these regional constraints,

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A Cordilleran B 30 N margin Franklinian margin Baltican & margin Caledonian PRA 0 Longshore currents terranes B.C. Ellesmere Is. Cal. Fig. 7C Fig. 7D Idaho Nevada Fig. 7A Middle Devonian Fig. 7B deformation N. Greenland in Purcell Laurentia Fig. 7D Mountains 0 Pioneer Mtns. Appalachian W. Newfoundland Laurentia margin Fig. 7E Middle to Late Ordovician Middle to Late Devonian C D

CH Okanagan high 30 N AA Purcell Mtns.

YT Slide Mtn. PE Ocean ? St. Mary-Moyie Ellesmerian transform 15 N QN Figure 10D orogeny

EK Pioneer NS Mtns. Copper Basin Gp. Antler orogeny Laurentia ans Snake River transfer AppalachiansAppalachi Late Devonian-Early Mississippian Late Devonian-Early Mississippian

Figure 10. Paleozoic paleogeography for Laurentia with focus on Cordilleran margin development. See text for explanation. (A) Middle to Late Ordovician time slice modified from plate reconstruction of van Staal and Hatcher (2010). Longshore currents along Cordilleran margin transport northwest Laurentian-affinity sediment from Peace River Arch (PRA) of northwestern Canada to the southwestern United States. B.C.—British Columbia; Is.—Island. (B) Middle to Late Devonian time slice modified from base map of Colpron and Nelson (2009). The northern margin of Laurentia is the site of a west-migrating subduction system. Sinistral fault system develops along Cordilleran margin and accommodates the southward displacement of some Baltican- and/or Caledonian-affinity terranes. Eifelian deformation in Purcell Mountains of southeastern British Columbia results from the interaction of Baltican- and/or Caledonian-affinity terranes and Cordilleran margin. Cal.— Caledonides. (C) Late Devonian to Early Mississippian time slice modified from base map of Colpron and Nelson (2009). Tectonic development of the Antler orogeny is linked to sinistral transcurrent system along western Laurentia. AA—Arctic Alaska; CH—Chukotka; EK—Eastern Klamath terrane; NS—Northern Sierra terrane; PE—Pearya terrane; QN—Quesnellia; YT—Yukon-Tanana terrane. (D) Speculative plate tectonic setting for the Pioneer Mountains region modified from Eisbacher (1983), Wilson et al. (1994), Link et al. (1996), and Lund (2008). Copper Basin depocenter is a releasing-bend basin bounded on the south by an uplifted restraining-bend of lower Paleozoic passive margin rocks and to the west by western Laurentian strata of the Roberts Mountain allochthon. Gp.—group.

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especially the stratigraphic framework of Wilson et al. (1994), we con- EAR-0838476 to Link. We greatly appreciate the help of George Gehrels, Mark Pecha, and staff at the NSF-supported (grant EAR-1338583) Arizona LaserChron Center. Constructive and thought- clude that Mississippian flysch successions of east-central Idaho were ful reviews by George Gehrels, Todd LaMaskin, and JoAnne Nelson improved this manuscript. deposited in a releasing bend basin that was bounded on the south by an uplifted restraining bend (Fig. 10D). REFERENCES CITED The releasing bend basin in the Pioneer Mountains was located imme- Albers, J.P., and Bain, J.H.C., 1985, Regional setting and new information on some critical geo- diately north of the Snake River transfer zone (Fig. 10D), a northeast- logic features of the West Shasta District, California: Economic Geology and the Bulletin of the Society of Economic Geologists, v. 80, p. 2072–2091, doi:10 .2113 /gsecongeo .80 .8 .2072. trending structural feature of the Laurentian craton in the Snake River Allen, P.A., Crampton, S.L., and Sinclair, H.D., 1991, The inception and early evolution of the Plain region of southern Idaho and northern Nevada (Lund, 2008). North of North Alpine foreland basin, Switzerland: Basin Research, v. 3, p. 143–163, doi:10 .1111 /j the Pioneer Mountains, we speculate that the northeast-trending St. Mary– .1365-2117.1991.tb00124.x. 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Anfinson, O.A., Leier, A.L., Gaschnig, R., Embry, A.F., and Dewing, K., 2012b, U-Pb and Hf iso- associated with the St. Mary–Moyie transform zone. It is therefore likely topic data from Franklinian Basin strata: Insights into the nature of Crockerland and the that future studies of Devonian–Mississippian strata in the northern U.S. timing of accretion, Canadian Arctic Islands: Canadian Journal of Earth Sciences, v. 49, and southern Canadian Rocky Mountains will discover new evidence for p. 1316–1328, doi:10.1139/e2012-067. Anfinson, O.A., Leier, A.L., Dewing, K., Guest, B., Stockli, D.F., and Embry, A.F., 2013, Insights mid-Paleozoic tectonism near long-lived basement structures. into the Phanerozoic tectonic evolution of the northern Laurentian margin: Detrital apatite and zircon (U-Th)/He ages from Devonian strata of the Franklinian Basin, Canadian Arctic CONCLUSIONS Islands: Canadian Journal of Earth Sciences, v. 50, p. 761–768, doi:10 .1139 /cjes -2012 -0177. Anfinson, O.A., Embry, A.F., and Stockli, D.F., 2016, Geochronologic constraints on the Perm- ian–Triassic northern source region of the Sverdrup basin, Canadian Arctic Islands: Tec- Paleozoic continental margin strata of the Pioneer Mountains, east- tonophysics, doi:10.1016/j.tecto.2016.02.041. central Idaho, have detrital zircon U-Pb age and Hf isotope signatures Baar, E.E., 2009, Determining the regional-scale detrital zircon provenance of the Middle-Late Ordovician Kinnikinic (Eureka) Quartzite, east-central Idaho, U.S. [M.S. thesis]: Pullman, that provide new constraints on the early growth and evolution of the Washington State University, 134 p. North American Cordillera. 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These results are consistent with widespread early Paleozoic sedi- Bahlburg, H., Vervoort, J.D., DuFrane, S.A., Carlotto, V., Reimann, C., and Cárdenas, J., 2011, The U-Pb and Hf isotope evidence of detrital zircons of the Ollantaytambo Formation, ment recycling along the western margin of Laurentia, analogous to the southern Peru, and the Ordovician provenance and paleogeography of southern Peru passive margin histories of northern and eastern North America after the and northern Bolivia: Journal of South American Earth Sciences, v. 32, p. 196–209, doi: break-up of supercontinent Rodinia. The passive to convergent margin 10.1016/j.jsames.2011.07.002. Beranek, L.P., Link, P.K., and Fanning, C.M., 2006, Miocene to Holocene landscape evolution transition in the northern U.S. Rocky Mountains occurred by Middle to of the western Snake River Plain region, Idaho: Using the SHRIMP detrital zircon prov- Late Devonian time, and is in part documented by west-derived Frasnian enance record to track eastward migration of the Yellowstone hotspot: Geological Society of America Bulletin, v. 118, p. 1027–1050, doi:10.1130 /B25896 .1. turbidite successions that shed Proterozoic and early Paleozoic detrital Beranek, L.P., Mortensen, J.K., Lane, L.S., Allen, T.L., Fraser, T.A., Hadlari, T., and Zantvoort, W.G., zircons into the Cordilleran margin system. The available detrital zircon Hf 2010, Detrital zircon geochronology of the western Ellesmerian clastic wedge, northwest- isotope data suggest that the western source for these Pioneer Mountains ern Canada: Insights on Arctic tectonics and the evolution of the northern Cordilleran miogeocline: Geological Society of America Bulletin, v. 122, p. 1899–1911, doi:10 .1130 /B30120 .1. strata was an early Paleozoic arc built on Proterozoic crust, with poten- Beranek, L.P., van Staal, C.R., McClelland, W.C., Israel, S., and Mihalynuk, M.G., 2013a, De- tial provenance regions in outboard basement complexes of the Eastern trital zircon Hf isotopic compositions indicate a northern Caledonian connection for the Klamath, Northern Sierra, and Quesnellia terranes. Mid-Paleozoic con- Alexander terrane: Lithosphere, v. 5, p. 163–168, doi:10 .1130 /L255 .1. Beranek, L.P., Pease, V., Scott, R.A., and Thomsen, T.B., 2013b, Detrital zircon geochronology vergent margin activity in east-central Idaho was related to the enigmatic of Ediacaran to Cambrian deep-water strata of the Franklinian basin, northern Ellesmere Antler orogeny and primarily preserved by a penetrative cleavage in Mil- Island, Nunavut: Implications for regional stratigraphic correlations: Canadian Journal ligen Formation strata and the rapid deposition of Mississippian flysch of Earth Sciences, v. 50, p. 1007–1018, doi:10.1139 /cjes -2013-0026. Beranek, L.P., Pease, V., Hadlari, T., and Dewing, K., 2015, Silurian flysch successions of Elles- in a hybrid, flexural- and fault-controlled foreland basin. Mississippian mere Island, Arctic Canada, and their significance to northern Caledonian palaeogeog- turbidite units contain recycled Precambrian detrital zircons and were raphy and tectonics: Journal of the Geological Society [London], v. 172, p. 201–212, doi: 10.1144/jgs2014-027. deposited in a releasing bend basin that was bounded on the south by an Berman, R.G., Ryan, J.J., Gordey, S.P., and Villeneuve, M., 2007, Permian to Cretaceous poly- uplifted restraining bend of lower Paleozoic passive margin rocks and to metamorphic evolution of the Stewart River region, Yukon-Tanana terrane, Yukon, Canada: the west by western Laurentian strata of the Roberts Mountain alloch- P-T evolution linked with in situ SHRIMP monazite geochronology: Journal of Metamor- phic Geology, v. 25, p. 803–827, doi:10.1111/j.1525-1314.2007.00729.x. thon. Sinistral-oblique tectonism is most consistent with mid-Paleozoic Boghossian, N.D., Patchett, P.J., Ross, G.M., and Gehrels, G.E., 1996, Nd isotopes and the plate tectonic scenarios that feature the north to south time-transgressive source of sediments in the miogeocline of the Canadian Cordillera: Journal of Geology, juxtaposition of the Quesnellia, Eastern Klamath, and Northern Sierra v. 104, p. 259–277. Bouvier, A., Vervoort, J.D., and Patchett, P.J., 2008, The Lu-Hf and Sm-Nd isotopic composi- basement terranes along the Cordilleran margin of western Canada and tion of CHUR: Constraints from unequilibrated chondrites and implications for the bulk western United States. These docked terranes subsequently formed part composition of terrestrial planets: Earth and Planetary Science Letters, v. 273, p. 48–57, of the crustal substrate to a west-facing continental arc that began rifting doi:10.1016/j.epsl.2008.06.010. Bradley, D.C., and O’Sullivan, P., 2016, Detrital zircon geochronology of pre- and syncollisional away in Mississippian time, creating a marginal ocean basin between the strata, Acadian orogeny, Maine Appalachians: Basin Research, doi:10 .1111 /bre.12188. fringing volcanic system and ancestral Pacific margin. Burchfiel, B.C., and Davis, G.A., 1972, Structural framework and evolution of the southern part of the Cordilleran orogeny, western United States: American Journal of Science, v. 272, p. 97–118, doi:10.2475/ajs.272.2.97. ACKNOWLEDGMENTS Burchfiel, B.C., and Davis, G.A., 1975, Nature and controls of Cordilleran orogenesis, western This work was conducted over several decades with the assistance of D.W. Rodgers, E. Wilson, United States: Extensions of an earlier synthesis: American Journal of Science, v. 272‑A, I. Warren, J. Preacher, and students of the 1993 Idaho State University geology field camp. p. 363–396. T. Armstrong, T. Diedesch, and J. Vogl collected some of the rock samples mentioned herein. Burchfiel, B.C., and Royden, L.H., 1991, Antler orogeny: A Mediterranean-type orogeny: Geol- Partial funding was provided by National Science Foundation (NSF) grants EAR-0510980 and ogy, v. 19, p. 66–69, doi:10.1130/0091-7613(1991) 019<0066:AOAMTO> 2.3.CO;2.

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