RESEARCH

Record of orogenic cyclicity in the Alberta foreland basin, Canadian Cordillera

Garrett M. Quinn1, Stephen M. Hubbard1, Reid van Drecht1, Bernard Guest1, William A. Matthews1, and Thomas Hadlari2 1DEPARTMENT OF GEOSCIENCE, UNIVERSITY OF CALGARY, EARTH SCIENCE 118, 2500 UNIVERSITY DRIVE NW, CALGARY, ALBERTA T2N 1N4, CANADA 2GEOLOGICAL SURVEY OF CANADA, 3303 33 STREET NW, CALGARY, ALBERTA T2L 2A7, CANADA

ABSTRACT

Jurassic–Cretaceous sedimentary rocks of the Alberta foreland basin are a key record of the evolution of the Canadian Cordillera. We test a recent model for cyclical development of Cordilleran orogenic systems using detrital zircon analysis of the major sandstone units deposited between 145 and 80 Ma exposed in the Rocky Mountain Foothills near Grande Cache, Alberta. The basin history is well constrained by decades of study, and the stratigraphy has been previously subdivided into tectonostratigraphic wedges. U-Pb data from 14 detrital zircon samples are included in this study. All the major magmatic provinces of North America are represented in each sample, with the relative proportions varying between samples. The samples are assigned to five groups with the aid of multidimensional scaling. Groups 1–3 are interpreted to record recycling from specific passive-margin units of western North America with varying input from the Cordilleran magmatic arc. Group 4 is interpreted to record recycling from sedimentary strata in the United States and dispersal by basin-axial fluvial systems. Group 5 is dominated by Mesozoic zircon grains interpreted to have originated in the Cordilleran magmatic arc. Detrital zircon age spectra do not form groups based on the tectonostratigraphic wedges from which they were sampled; rather, within each tectonostratigraphic wedge, they exhibit evolution from diverse age spectra to a less-diverse distribution of detrital zircon ages. We constructed a proxy for magmatic flux of the Cordilleran magmatic arc using detrital zircon ages younger than 200 Ma; it shows three modes at ca. 165, 115, and 74 Ma. These ages are considered high-flux episodes of magmatism that are linked to cyclical uplift and plateau formation in the orogen. This cyclical process is interpreted to: (1) control sedimentation rates in the foreland; (2) account for evolving provenance by altering catchments; and (3) be a plausible mechanism for the deposition of the tectonostratigraphic wedges in the Alberta foreland basin.

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INTRODUCTION (Bally et al., 1966; Monger et al., 1972; Monger sediments throughout the stratigraphic section and Price, 1979; Coney et al., 1980; Beaumont, remains poorly documented. In this study, we Recent models of cyclical orogenic devel- 1981; Monger et al., 1982; Stott, 1984; Cant analyzed every significant sandstone unit depos- opment attempt to describe a unifying frame- and Stockmal, 1989; Leckie and Smith, 1992). ited between 145 and 80 Ma from the Grande work of interrelated crustal processes, including The Alberta foreland basin formed and filled Cache area of the central Alberta Foothills using underthrusting, eclogite root foundering, crustal in response to tectonic loading of the western U-Pb geochronology of detrital zircon grains. shortening, episodic magmatism, and plateau margin of North America by allochthonous and We tested the hypothesis of orogenic cyclicity development and collapse (DeCelles et al., 2009; parautochthonous terranes starting in the Middle in western Canada through analysis of detrital Vanderhaeghe, 2012). Inherently, these models Jurassic (Monger et al., 1972, 1982; Monger and zircon spectra in the context of a high-resolu- predict episodic sedimentation in foreland basins. Price, 1979). Docking of terranes to the North tion stratigraphic framework from this uniquely As such, foreland basin strata are a key archive American margin progressed until the Eocene, well-constrained foreland basin. in which to sample Cordilleran magmatic arcs resulting in a complex orogenic collage (Monger and test orogenic cyclicity hypotheses. et al., 1972; Coney et al., 1980). STRATIGRAPHIC CONTEXT AND The western North American foreland basin Numerous authors have recognized the cycli- STUDY AREA extends from southern Mexico to the Canadian cal nature of Alberta foreland basin strata and Arctic, ~6000 km along strike, with a maximum subdivided the fill into lithostratigraphic cycles The stratigraphic framework for siliciclas- width exceeding 1000 km (DeCelles, 2004). The or tectonostratigraphic wedges (Stott, 1984; tic Mesozoic units in the Alberta foreland basin Alberta foreland basin is the portion of this basin Cant and Stockmal, 1989; Leckie and Smith, has been extensively analyzed, with several occupying the Canadian province of Alberta. 1992; Ross et al., 2005; Pana and van der Pluijm, studies emphasizing the linkage of sedimentary The Canadian Cordillera and the Alberta fore- 2015). The paleogeographic evolution of the packages to tectonic processes in the adjacent land basin are exceptionally well studied due to basin is well understood, providing constraints Canadian Cordillera (Fig. 1; Table 1; Cant and expansive outcrops and hundreds of thousands on accommodation development and sediment- Stockmal, 1989; Ross et al., 2005; Raines et al., of well penetrations. This linked orogen-basin routing variation (Jackson, 1984; Leckie and 2013; Pana and van der Pluijm, 2015). The stra- system is the focus of classic works on accre- Smith, 1992). tigraphy of the Alberta foreland basin consists tionary margin tectonics, fold-and-thrust belts, Despite this well-established framework of unconformity- or flooding surface–bounded basin analysis, stratigraphy, and sedimentology for the Alberta foreland basin, the origin of sequences, which are variably subdivided into

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Terrane Grande Leckie and Cant and Ross et al. Pana and van Accretion Cache Smith Stockmal (2005) der Pluijm Events Age Stratigraphy (2015) Price et al. (Ma) (1992) (1989) (1981) Maastrichtian Paci c Rim/ Tectono- Chuga 72.1 Saunders Cycle 4 stratigraphic Campanian Group Wedge 4 Insular Pulse 3 Superterrane Late 83.6 Santonian 86.3 Smoky Coniacian Quiescence 89.8 Group Turonian Cycle 3 Oblique 93.9 ompression Cenomanian Dunvegan Fm. T.W. 3 C 100.5 Ft. St. John Quiescence Cascadia Albian Group

Cretaceous Pulse 2 113.0 Tectono- Cycle 2 stratigraphic e Aptian Wedge 2 Bullhead onic Early Group 125.0 Erosion Barremian and Tect 129.4 Bridge River Hauterivian Quiescenc 132.9 Reworking Valanginian 139.8 Berriasian Monteith 145.0 Formation Tithonian 152.1 Late Kimmeridgian 157.3 Tectono- Oxfordian Intermontane Fernie Cycle 1 stratigraphic Pulse 1 Superterrane 163.5 Wedge 1 ompression Callovian 166.1 Formation C Middle Bathonian 168.3 Bajocian 170.3 Aalenian 174.1

Toarcian Initial Jurassic 182.7 Emplacement Pleinsbachian of Allochtho- Early 190.8 nous Terranes Sinemurian 199.3

Figure 1. Tectonostratigraphic and lithostratigraphic cycles in the Alberta foreland basin compared to the stratigraphic column of lithostratigraphic units considered in this study. Diamonds indicate units sampled. See Table 1 for detailed stratigraphic and sampling information. T.W.—tectonostratigraphic wedge.

tectonostratigraphic wedges or lithostratigraphic deposits are represented by the Monteith Forma­ River terrane to the margin of North America at cycles (Fig. 1; Stott, 1984; Cant and Stockmal, tion of the Minnes Group, which represents a this time has been linked to deposition of these 1989; Leckie and Smith, 1992; Ross et al., 2005; progradational package of deltaic to fluvial sedi- sediments (Price et al., 1981; Rusmore et al., Pana and van der Pluijm, 2015). These cycles ments (Miles et al., 2012; Kukulski et al., 2013a). 1988; Cant and Stockmal, 1989). provide the framework for the timing of sedimen- The basal bounding surface of the second There is disagreement as to whether the tation and hiatus events, which can be compared tectonostratigraphic wedge is the basinwide sub- Cadotte Member of the Peace River Forma- to tectonic events in the Canadian Cordillera. Cretaceous unconformity, which represents a tion (Fort St. John Group) is part of the sec- Jurassic to earliest Cretaceous deposits in 10–20 m.y. hiatus attributed to isostatic rebound ond tectonostratigraphic wedge or should be the basin are widely assigned to the first tec- during an extended period of tectonic quies- considered as part of an intervening period of tonostratigraphic wedge or depositional cycle in cence (Heller et al., 1988; Cant and Stockmal, tectonic quiescence (Table 1; Cant and Stock- the basin. Protracted subsidence and sedimen- 1989). The Bullhead Group, basal Fort St. John mal, 1989; Leckie and Smith, 1992). Gouge of tation are linked to loading of the lithosphere Group, and equivalents are assigned to the sec- comparable age was absent from major thrust by accretion of the Intermontane superterrane ond cycle of sedimentation in the basin (Table faults in the Rocky Mountains, consistent with to the western margin of North America (Cant 1; Cant and Stockmal, 1989; Leckie and Smith, the tectonic quiescence hypothesis (Pana and and Stockmal, 1989). In the study area, these 1992; Ross et al., 2005). Accretion of the Bridge van der Pluijm, 2015).

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TABLE 1. SUMMARY OF PUBLISHED INFORMATION ON INDIVIDUAL UNITS SAMPLED, CALCULATED MAXIMUM DEPOSITIONAL AGES AND DETRITAL ZIRCON AGE MODES. Max Dep. Youngest Tectonic Signicance Unit Reported Dep. Orogenic Group Age (2σ) Grain (Cant and Stockmal, Sampled Age (Ma) Events (Can. Lexicon ) (Ma) (Ma) 1989, Ross et al., 2005) Dynamic subsidence induced Chinook Mb. 82±1.3 by foundering of the subducted Smoky Gp. 99.6-65.5 79±2.5 (Puskwaskau Fm.) (11) slab

95±2.5 Smoky Gp. Tectonic quiescence Cardium Fm. 99.6-65.5 (6) 92±4.4

Cascadia terrane accretion Late Cretaceous clastic wedge 371±29 Dunvegan Fm. 99.6-93.6 96±6.2 Renewed uplift and denudation of (3) the orogen

Sub-Paddy Unconformity ca. 5 m.y.

Cadotte Mb. 382±9.8 Tectonic quiescence Ft. St. John Gp. 108.8-106.4 110±4.1 (Peace River Fm.) (4)

Stikinia terrane accretion High accommodation; signi cant Notikewin Mb. Ft. St. John Gp. 112.0-99.6 110±1.9 pulse of sediment supply from the (Spirit River Fm.) (10) 107±4.1 orogen

High accommodation; signi cant Falher A Mb. 111±11 pulse of sediment supply from the Ft. St. John Gp. 112.0-99.6 100±5.5 (Spirit River Fm.) (3) orogen

High accommodation; signi cant Falher D Mb. 111±4.2 pulse of sediment supply from the Ft. St. John Gp. 112.0-99.6 orogen (Spirit River Fm.) (4) 106±13.0

Lower Cretaceous clastic wedge; Bluesky Fm. Ft. St. John Gp. 112.0-108.8 114±1.6 Beginning of a major trangression (3) 91±1.9 related to increasing accommodation

Lower Cretaceous clastic wedge; 375±17.0 Gething Fm. Bullhead Gp. 130.0-108.8 elevated accommodation (4) 116±3.2

117±1.7 Bridge River terrane accretion Lower Cretaceous clastic wedge; Bullhead Gp. 145.5-108.8 115±3.7 Cadomin Fm. (4) period of uplift

Sub-Cretaceous Unconformity ca. 10-20 m.y.

Continued accretion of the Jurassic clastic wedge; Monteith A Mb. 199±9.1 Intermontane superterrane and elevated denudation and Minnes Gp. 146.0-125.0 196±11.6 (Monteith Fm.) (3) uplift and denudation of the coarse-grained sediment transfer Omineca belt to foredeep

Monteith B Mb. 296±20.0 Minnes Gp. 146.0-125.0 129±3.6 (Monteith Fm.) (3)

Intermontane superterrane Jurassic clastic wedge; Monteith C Mb. Minnes Gp. 146.0-125.0 162±9.6 (Monteith Fm.) 143±3.1 accretion rst coarse clastic sediments (4) in the foreland basin

(continued)

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TABLE 1. SUMMARY OF PUBLISHED INFORMATION ON INDIVIDUAL UNITS SAMPLED, CALCULATED MAXIMUM DEPOSITIONAL AGES AND DETRITAL ZIRCON AGE MODES (continued).

Paleogeographic Context Depositional Prominent DZ -age peaks in Additional References (Leckie and Smith, 1992) Environments order of prominence (Ma)

Shoreline prograding northeastward to Storm-dominated 84, 161, 197, 406, 1762, 1029, 1911 Lerand, 1983; Leckie, 1989; Beaumont et al. shallow seaway shoreline/shelf progradational 1993; Collom, 2001; Benham and Collom, 2012 cycles

Shoreline prograding northeastward to Shoreface progradational 120, 96, 431, 1800, 1755, 1058, 2022 Walker, 1983; Shank and Plint, 2013 shallow seaway cycles

Major deltaic system prograding Deltaic progradational cycles 1768, 423, 200, 112, 1028, 2660 Bhattacharya et al., 1994; Plint, 2000 southeastward to shallow seaway

Sub-Paddy Unconformity ca. 5 m.y.

Northwest-southeast trending shoreline Interdeltaic shoreline 436, 594, 110, 380, 324, 1674, 1196, Smith et al., 1984; Rahmani and Smith, 1988 that prograded to north-northeast into 1734, 1046, 1488 shallow seaway

Northward-trending river systems with 165, 109, 214 Monger and Price, 1979; Smith et al., 1984; coeval shorelines/delta plain in northern Leckie, 1985 Alberta/British Columbia

Northward-trending river systems with 166, 115, 415, 484, 591, 290, 1040, Smith et al., 1984; Rahmani, 1984; Youn, 1983 coeval shorelines/delta plain in northern 1690, 1869 Alberta/British Columbia

Northward-trending river systems with 110, 1845, 168, 238, 428, 1017, 618, Smith et al., 1984; Leckie, 1986; Jackson, 1984; coeval shorelines/delta plain in 1635 Casas and Walker, 1997; Wadsworth et al., northern Alberta/British Columbia 2003

Shoreline of shallow intercontinental Marginal marine, barrier bar 114, 1761, 1803, 627, 195 Smith et al., 1984; Chiang, 1984; sea transgressing from the north McLean and Wall, 1981

1788, 117, 440, 384, 1035, 632, 1108, Smith et al., 1984; Langenberg et al., 1997 variably coal-forming 199, 1481 northwestward intersected by tributaries from orogenic belt

Dissected piedmont with axially oriented Braided river plain 117, 1835, 185, 260, 592 Monger and Price, 1979; Gies, 1984; Smith et al., 1984; Heller et al. 1988; intersected by tributaries from orogenic Leier and Gehrels, 2011 belt

Sub-Cretaceous Unconformity ca. 10-20 m.y.

1843, 1920, 2077, 1037, 200, 2709 Miles et al., 2012; Kukulski et al., 2013a, 2013b; northeastward coalescing channel belts Raines et al., 2013

397, 616, 578, 431, 129, 141, 166, 285, 1027, 1165, 1536, 2068

Storm dominated delta 588, 560, 398, 166, 143, 366, 309, 1130, Miles et al., 2012; Raines et al., 2013 north-northwestward 1038, 1666, 1862, 2076 Raines et al. (2013): 422, 1051, 166, 348, 1792, 454, 1326, 2713, 1707, 1881, 1508, 292 1Lexicon of Canadian Geological Names. Available at http://weblex.rncan.gc.ca/weblexnet4/weblex_e.aspx. 2The number of youngest zircon grains that were averaged to produce the maximum depositional age is in parentheses. 3Detrital zircon

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The Dunvegan Formation represents a major previously published data from the Monteith has been widely applied, it perhaps incorrectly deltaic system that is assigned to the third tec- C and A members (Raines et al., 2013). Two assumes that the youngest overlapping grains tonostratigraphic wedge (Fig. 1; Cant and Stock- samples were analyzed from the Barremian– are comagmatic (cf. Spencer et al., 2015a). mal, 1989; Bhattacharya, 1994; Plint, 2000). Aptian Bullhead Group, including the Cadomin Although future analyses should perhaps con- Deposition of the Dunvegan Formation has been and Gething Formations. Five samples were col- sider this approach, the method of Dickinson linked to accretion of the Cascadia terrane and lected from Albian–Cenomanian sandstones of and Gehrels (2009) is deemed adequate for the a period of oblique compression (Price et al., the Fort St. John Group, including the Bluesky level of interpretation utilized in this study. 1981; Cant and Stockmal, 1989; Pana and van Formation, the Falher and Notikewin Members Multidimensional scaling (MDS) is used der Pluijm). of the Spirit River Formation, and the Cadotte to aid in the visualization and interpretation of The Smoky Group is not included in the third Member of the Peace River Formation. One statistical differences in detrital zircon spectra. tectonostratigraphic wedge but is rather linked sample was collected from the Cenomanian MDS creates a map of the data points based on to a time of quiescence in the orogen (Cant and Dunvegan Formation and two from the Ceno- the D values that are produced as part of the Stockmal, 1989). There are no fault gouge ages manian–Campanian Smoky Group (Cardium Kolmogorov-Smirnov test (Vermeesch, 2013; that overlap this time interval (Pana and van der Formation and the Chinook Member of the Spencer and Kirkland, 2016). The D value repre- Pluijm, 2015). Puskwaskau Formation; Fig. 3). sents the maximum vertical separation between A fourth major clastic wedge is widely Sandstone samples, 3 to 4 kg each, were pul- two cumulative density functions. These “dis- reported for the basin (Fig. 1). Campanian to verized, and density separation was performed tances” are arranged in a matrix, which is then Paleocene sediments of the Saunders Group and on an MD Gemini Goldharvester™ shaking represented in two-dimensional space such that equivalents, including the Belly River Group, table (water table). Zircon grains were further all the “distances” in the matrix are honored. Edmonton Group, and Paskapoo Formation, concentrated using heavy liquids. Magnetic Uncertainties are not considered in this analysis. record the last major phase of foreland sedi- separation was followed by dump-mounting of Limitations of using the D value include the fol- mentation (Cant and Stockmal, 1989; Leckie grains in 2.5-cm-diameter epoxy puck mounts, lowing: (1) It is known to have higher sensitivity and Smith, 1992; Ross et al., 2005). This stra- which were ground to expose the zircon grains to differences in the cumulative density func- tigraphy is dominantly nonmarine and has been and polished. U-Pb age analysis was performed tions near the median; (2) it is more sensitive linked to accretion of the Insular superterrane, at the Centre for Pure and Applied Thermochro- to proportions of ages rather than the mean age Pacific Rim terrane, and Olympic terrane (Price nology and Tectonics (CPATT) at the Univer- of the mode; and (3) it is not as robust when et al., 1981; Cant and Stockmal, 1989; Leckie sity of Calgary using laser ablation–inductively comparing small data sets (n < 300–600; Saylor and Smith, 1992). This tectonostratigraphic coupled plasma–mass spectrometry (LA-ICP- and Sundell, 2016). Despite these limitations, wedge was not sampled because the strata are MS). The zircon grains were analyzed using a 22 MDS provides reasonable groupings in this data not exposed in the Grande Cache area. µm spot diameter. Four zircon references were set. Unimodal, normally distributed age popula- Grande Cache, located in the Rocky Moun- ablated along with the unknowns to correct for tions were created in Excel™ and added to the tain Foothills of west-central Alberta, is an ideal laser-induced elemental fractionation, instru- MDS map to show key inputs to the various place in which to evaluate the provenance evo- mental fractionation, drift, and to test the accu- groups. A Matlab™ code and a graphical-user lution in the Alberta foreland basin for three racy of the laser-ablation procedure (Temora-2— interface made available by Vermeesch (2013) reasons: (1) Nearly every significant sandstone Black et al., 2004; 91500—Wiedenbeck et al., were used to perform the MDS analysis and cre- of the foreland basin sequence from 145 to 80 1995; FC-1—Paces and Miller, 1993; 1242— ate the plots. The matrix of D values from the Ma crops out within 15 km of the townsite. (2) Mortensen and Card, 1993). Data reduction Kolmogorov-Smirnov test is included in the data Research focused on the structural geology of was performed in Iolite™ V2.5 following the repository item (see footnote 1). the area constrains the distribution and geo- methodology of Paton et al. (2010), using com- logical history of the units investigated (e.g., ponents of the Vizualage data reduction scheme RESULTS Mountjoy, 1980; McMechan, 1999). (3) Vari- (Petrus and Kamber, 2012). Final assessment of ous stratigraphic, sedimentologic, and paleon- uncertainty and data visualization were done in Prominent detrital zircon age modes, maxi- tologic studies have characterized units in the Excel™ using Isoplot (Ludwig, 2012). All ages mum depositional ages, depositional environ- area (Fig. 2; e.g., Plint, 2000; Collom, 2001; are reported as concordia ages (Ludwig, 1998). ments, paleogeographic context, tectonic sig- Kukulski et al., 2013b; McCrea et al., 2014). Errors are quoted at the 2σ level. Full isotopic nificance, and concurrent orogenic events are data and details of the analytical method can be reviewed for each of the stratigraphic horizons METHODS found in the GSA Data Repository.1 sampled in Table 1. The age modes referenced Maximum depositional ages were calculated in Table 1 are reported in order of prominence. Strata were sampled within 15 km of Grande as the weighted average of the youngest subset Probability density plots for each of the samples Cache, primarily within the Muskeg thrust of zircon grains that overlapped in age at 2σ are presented in Figure 4. (Fig. 2; Irish, 1951; Richardson et al., 1991; error (Dickinson and Gehrels, 2009). At mini- Jurassic–earliest Cretaceous strata that com- McMechan, 1996; McMechan and Wozniak, mum, three overlapping zircon ages were used prise the first tectonostratigraphic wedge have 1996). The stratigraphic context for samples in each case. The youngest single grain in each age modes spanning the Mesozoic to Archean analyzed is presented in Figure 3. sample is also reported, with the correspond- (Fig. 4). Similarities between the samples Four sandstones of Jurassic to earliest Cre- ing error at the 2σ level. Although this method include modes in the Paleozoic (ca. 430 Ma), taceous age from the Monteith Formation of early Mesoproterozoic (ca. 1000 Ma), the Paleo- the Minnes Group are included in this study. 1 GSA Data Repository Item 2016148, a detailed proterozoic (ca. 1800 Ma), and the Archean (ca. The informal Monteith C and Monteith B mem- description of the analytical methods used and U-Pb 2700 Ma). The major difference between these isotopic data and ages of detrital zircon grains, is avail- bers were analyzed as part of this study (Miles able at www.geosociety.org/pubs/ft2016.htm, or on samples is the proportion of ages from the et al., 2012). These data are augmented with request from [email protected]. various age groups. The Monteith C member

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Moreley N ALBERTA

We st Outpick 54°07’N Thrust

Grande Cache Thrus Study Area t 200 km Calgary East Cut Copton Thrust

Thrust Cutpick Thrust 40

y River Muskeg Smok Thrus t Fold-Thrust Belt Stable North Fahler (A and D) America Notikewan Canada 54°00’N Bluesky Cadotte USA

Laramide Foreland Province Basin

N 500 km Mexico Monteith B Maso n Monteith C Thrust Muskeg

Thrust Chinook Cow lic k 40 Th Cardium rus t Gething Cadomin

53°53’N Sulphur River GRANDE Dunvegan CACHE

Thrust Ster ne Falut Ma non Fa ult 119°10’W 119°00’W 5 km

Pleistocene and Recent (Qvf) Chungo Mem (Kpc) Cardium Fm ( Kca) Bluesky Fm (Km) Wapiti Group (KPc-l) (Kpd) Gething Fm (Kgi) -Coalspur Fm Kaskapau Fm (Kk) Dowling Mem Cadomin Fm (Kc) Thistle Mem Dunvegan Fm (Kd) Brazeau Fm (Kbz-l - Kbz -u) Hanson Mem Minnes Group (Kgc) Marshybank Fm (Kma) Shaftesbury Fm (Ks) Jkmts Monteith Fm Puskwaskau Formation Spirit River Group (Kg) Muskiki Fm ( Kmu) Jkmtm Nomad Mem (Kpn) -Wilrich Mem JKn Geological Boundary -Falher Mem -Notikewin Mem Thrust Fault (de ned, assumed)

Figure 2. Simplified geological map of Grande Cache and surrounding area, including sample locations (after McMechan, 1996; McMechan and Wozniak, 1996; Richardson et al., 1991; Irish, 1951). Inset map shows the location of Grande Cache in context of North America (modified after DeCelles, 2004).

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NORTHERN NORTHWEST Age MOUNTAINS AND MOUNTAINS AND Depth (Ma) FOOTHILLS PLAINS Gamma-Radiation (m) 56 (API) 0 150 PALEO- PASKAPOO Chinook Mbr. CENE ALEOGEN E P 66 COALSPUR UNDERS

SA BRAZEAU WAPITI Cardium Fm.

2000 NOMAD AU

UPPER CHUNGO CHINOOK ASK HANSON W THISTLE PUSKWASKAU Y Y PUSK DOWLING MARSHYBANK BAD HEART MUSKIKI MUSKIKI SMOK SMOK CARDIUM CARDIUM KASKAPAU KASKAPAU CEOUS POUCE COUPE DOE CREEK TA DUNVEGAN DUNVEGAN

CRE 101 SHAFTESBURY SHAFTESBURY Dunvegan Fm. 2500 PADDY

. JOH N BOULDER CREEK . JOH N PEACE RIVER CADOTTE UPPER HULCROSS MOUNTAIN PARK HARMON FORT ST FORT ST NOTIKEWIN A GATES GRANDE CACHE SPIRIT OON RIVER FALHER to LOWER L RIVER F

OWER TORRENS L WILRICH MOOSEBAR BLUESKY Cadotte Mbr. GETHING GETHING Notikewin Fm. CADOMIN CADOMIN Fahler Fm. BULLHEA D BULLHEA D 3000 A A B B MONTEITH/ MONTEITH/ NIKANASSIN C NIKANASSIN C

145 MINNES MINNES

Bluesky Fm.

UPPER Gething Fm. 164 FERNIE FERNIE MIDDLE Cadomin Fm. 174 Monteith Fm. JURASSIC

OWER 3500 L

201

- Conglomerate and sandstone - Sandstone and siltstone commonly interbedded with shale - Detrital Zircon Sample - Shale and mudstone with subordinate siltstone

Figure 3. Stratigraphic chart showing nomenclature for the Foothills outcrop belt and adjacent subsurface (modified from Alberta Geologi- cal Survey, 2015). Sample locations are shown with diamonds. Gamma-ray log from well 00/07-02-063-08W6/00 illustrates thicknesses of units in the basin. In this study, nomenclature from the basin is used.

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the Notikewin Member sample, age modes in Chinook (n=132) the Paleozoic (ca. 400 Ma), the early Mesopro- terozoic (ca. 1000 Ma), and the Paleoprotero- zoic (ca. 1800 Ma) are also common between Cardium (n=83) the samples. The Cadomin Formation sample is dominated by a Cretaceous mode at 117 Ma Dunvegan (n=128) and a Paleoproterozoic mode at ca. 1840 Ma. The Gething Formation has similar modes to the Cadomin Formation at 117 Ma and ca. 1790 Cadotte (n=126) Early-Late Cretaceous Ma; however, the Gething Formation has a more prominent early Mesoproterozoic mode at 1108 Ma. The Bluesky Formation is most similar to Notikewin (n=138) the Cadomin Formation in that it is dominated by modes in the Cretaceous (114 Ma) and the Falher A (n=138) Paleoproterozoic (ca. 1760 Ma and ca. 1800 Ma). The overlying Falher D Member has a slightly broader spectrum of ages in the Pro- Falher D (n=67) terozoic and a higher proportion of Mesopro- terozoic zircon grains than the Bluesky Forma- tion. The Falher A Member is unique due to the Bluesky (n=95) high proportion of Paleozoic to Neoproterozoic grains (300–600 Ma). Likewise, the Mesopro- Early Cretaceous Gething (n=132) terozoic mode at 1040 Ma is more prominent in the Falher A Member than the Paleoproterozoic mode at ca. 1850 Ma. The Notikewin Member Cadomin (n=146) is dominated by Mesozoic zircon grains with modes at 165 Ma, ca. 110 Ma, and ca. 210 Ma. Proterozoic detrital zircon grains with similar Monteith A, Raines et al. (n=99) ages to the other samples were analyzed from the Notikewin Member sample, but the modes Monteith B (n=134) are muted because of the number of Mesozoic zircon grains (Fig. 4). Early–Late Cretaceous strata include age Monteith C (n=115) modes spanning the Mesozoic to the Archean (Fig. 4). The four samples also share age modes in the Mesozoic (110–120 Ma), the Paleozoic Monteith C, Raines et al. 2013 (n=79) (400–500 Ma), the Mesoproterozoic (1000 Ma),

Jurassic-Early Cretaceous and the Paleoproterozoic (1600–1800 Ma). The Cadotte Member and Dunvegan Formation con- 0 500 1000 1500 2000 2500 3000 3500 tain lesser proportions of Mesozoic zircon grains Age (Ma) than the Cardium Formation and Chinook Mem- ber samples. The Cadotte Formation exhibits Cordilleran Orogen (<250 Ma) Granite-Rhyolite Province (1.3–1.4 Ga) Appalachian Orogen (285–850 Ma) Yavapai-Mazatzal (1.6–1.8 Ga) a prominent mode in the Paleozoic at ca. 440 Grenville Orogen (1.0–1.3 Ga) Trans-Hudson Orogen (1.7–1.8 Ga) Ma, and the Proterozoic zircon grains are evenly distributed between the Mesoproterozoic and Figure 4. Probability density plots of detrital zircon grains sampled through the entire stratigraphic Paleoproterozoic, with age modes at ca. 1670, column exposed at Grande Cache. The colors of the probability density plots correspond to tec- ca. 1200, ca. 1730, ca. 1050, and ca. 1490 Ma, tonostratigraphic wedges of Cant and Stockmal (1989). The uncolored probability density plots in order of decreasing prominence. The Dun- (i.e., Cadotte, Cardium, Chinook) correspond to units not assigned to a tectonostratigraphic wedge by Cant and Stockmal (1989). vegan Formation is distinct from the Cadotte Member in that the mode at ca. 1770 Ma domi- nates the Proterozoic detrital zircon spectra. The analysis of Raines et al. (2013) is unique in that Monteith A member sample analysis of Raines Proterozoic detrital zircon grains in the Chinook the Proterozoic is characterized by more numer- et al. (2013) is unique in that it is dominated by Member and Cardium Formation are evenly dis- ous and prominent modes than the other samples. a strong age mode in the Paleoproterozoic at ca. tributed between the Mesoproterozoic and the This is evident in important modes centered at 1840 Ma (Fig. 4). Paleoproterozoic, though the mode at 1800 Ma ca. 1050 Ma, ca. 1325 Ma, ca. 1510 Ma, and ca. Early Cretaceous strata comprising the sec- in the Cardium Formation is somewhat more 1790 Ma. The Monteith C and Monteith B mem- ond tectonostratigraphic wedge have detrital zir- prominent (Fig. 4). ber samples are unique in that Paleozoic and con ages spanning the Mesozoic to the Archean Incorporation of progressively younger zir- Neoproterozoic modes are more important con- (Fig. 4). All six samples share a similar age con grains occurs up stratigraphic section (Fig. stituents, including ages at ca. 550–600 Ma. The mode in the Jurassic at ca. 160 Ma. Excluding 4). However, the youngest age mode is not

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always dominant. In the case of the early Albian In most instances, the biggest difference The western margin of North America is Notikewin Member, Middle Jurassic detrital between individual zircon age spectra is not host to thick packages of sedimentary rocks that zircon grains compose most of the sample; the the presence of a particular mode but the pro- accumulated in rift, passive-margin, and fore- Cenomanian Cardium Formation has a most portions of age groups (Fig. 4). Many of the land basin settings from the Mesoproterozoic prominent Aptian age mode (120 Ma). In the age spectra have relatively evenly distributed to the Triassic (Price et al., 1972; Root, 2001; Chinook Member, however, near-depositional- proportions among the Mesozoic, Paleozoic, Dickinson, 2004). These strata were uplifted age detrital zircon grains dominate (84 Ma). and the three eras of the Proterozoic. There are during the Cordilleran orogeny and contributed The ultimate source areas of detrital zir- important exceptions, however. For example, a diverse array of detrital zircon grains to the con grains in these strata reflect the Archean– the Monteith A member is composed of 51% Alberta foreland basin (Fig. 5; Ross and Ville- Mesozoic magmatic history of North America. Trans-Hudson–age detrital zircon grains, and neuve, 2003; Lewis et al., 2010; Leier and Geh- Archean zircon grains originated during the the Notikewin Member is composed of 75% rels, 2011; Raines et al., 2013; Laskowski et al., formation of the cratonic nucleus of North Cordilleran zircon grains. The Cardium Forma- 2013; Gehrels and Pecha, 2014). America (Hoffman, 1988). Paleoproterozoic tion and Chinook Member are less dominated A widely interpreted mechanism for west- detrital zircon grains are associated with sev- by Cordilleran influence, composed of 16% and ward transportation of Appalachian and Grenville eral orogenic sources that sutured the Archean 18% Cordilleran zircon grains, respectively. detritus from eastern to western North America cratons of North America (Hoffman, 1988; The detrital zircon age spectra do not form are continental-scale paleorivers (Rainbird et al., Whitmeyer and Karlstrom, 2007). Detrital zir- groups based on their assignment into lithostrati- 1992; Dickinson and Gehrels, 2009; Dickinson con age modes between 1800 and 1900 Ma are graphic groups nor the tectonostratigraphic et al., 2010; Benyon et al., 2014, 2016; Blum referred to as Trans-Hudson grains, though there wedges that have been interpreted by numer- and Pecha, 2014; Finzel, 2014). In addition to are other Paleoproterozoic orogens that have ous authors (Figs. 1 and 3; Stott, 1984; Cant Mesoproterozoic–Triassic passive-margin strata, magmatic assemblages of a similar age (Hoff- and Stockmal, 1989; Leckie and Smith, 1992; a relevant sink for these sediments was vast eolian man, 1988; Whitmeyer and Karlstrom, 2007). Ross et al., 2005). Jurassic to earliest Cretaceous deposits in the southwestern United States, and The Yavapai-Mazatzal Provinces contributed rocks of the first tectonostratigraphic wedge these were likely an important source of detri- Paleoproterozoic zircon grains that are younger are characterized by detrital zircon grains that tal zircon grains to the Western Interior Basin than the Trans-Hudson orogen, at 1610–1790 evolve from a broad age spectra to one domi- (Dickinson and Gehrels, 2009; Leier and Gehrels, Ma (Hoffman, 1988). Mesoproterozoic detrital nated by Trans-Hudson ages (Fig. 4). Follow- 2011; Laskowski et al., 2013; Raines et al., 2013). zircon grains with ages from 1340 to 1480 Ma ing the 10–20 m.y. hiatus of the sub-Cretaceous Northern sources of detrital zircon grains originated from the midcontinent belt of anoro- unconformity, the second tectonostratigraphic exist in the North American passive margin genic plutons known as the Granite-Rhyolite wedge evolves from broad age distributions (Lemieux et al., 2011; Hadlari et al., 2012; Geh- Province (Windley, 1989). The Grenville oro- in the Bullhead Group and basal Fort St. John rels and Pecha, 2014). However, these sources gen (ca. 1000–1300 Ma) contributed Mesopro- Group to a Mesozoic-dominated signature in the are discounted because the basin configura- terozoic detrital zircon grains that are common Notikewin Member (Fig. 4). The units from the tion was dominated by south to north sediment in this study; the Grenville magmatic pulse at uppermost stratigraphy studied exhibit a simi- transport during the Mesozoic (Jackson, 1984; 1040 Ma is particularly well represented (Easton, lar pattern, evolving from broad age spectra in Leckie and Smith, 1992). 1986; Dickinson, 2008). Younger Proterozoic the Cadotte Member and Dunvegan Formation To aid provenance interpretations, five zircon ages are associated with allochthonous to one dominated by Mesozoic modes (Fig. 4). provenance groups were established with the terranes of the Appalachian orogeny, specifi- aid of multidimensional scaling. This analysis cally the Brasiliano and Pan-African orogens ANALYSIS AND INTERPRETATION relies on incorporating nearest-neighbor lines of Gondwana (550–850 Ma; Park et al., 2010). to define the groups of related spectra, and syn- Other Appalachian and pre-Appalachian rift In the context of the assembly of North thetic end-member populations to show impor- magmatic assemblages span the Paleozoic to America, the Cordilleran orogen and foreland tant inputs to each group (Fig. 6). Neoproterozoic (285–760 Ma; Dickinson and basin system are young. The ultimate zircon Gehrels, 2009; Park et al., 2010). sources can be linked to the Alberta foreland Group 1: Trans-Hudson–Dominated Mesozoic detrital zircon age modes can be basin directly via continent-scale Jurassic–Cre- Spectrum with Minor Cordilleran Arc attributed to the magmatic arcs and accreted ter- taceous–age sediment routing systems (e.g., ranes that constitute the Cordilleran orogen to Raines et al., 2013; Benyon et al., 2014, 2016; This group includes only the Monteith A the west. Triassic plutons do not exist on pre- Blum and Pecha, 2014) or indirectly through member (Fig. 6). The detrital zircon spectrum Cordilleran North America; however, igneous one or more phases of sediment recycling (e.g., is characterized by a prominent Trans-Hudson and sedimentary units of this age are common Dickinson and Gehrels, 2009; Gehrels and age at ca. 1850 Ma, with a subordinate mode at to accreted terranes (e.g., Armstrong, 1988; Pecha, 2014; Hadlari et al., 2015). Recycling ca. 2080 Ma. This sample has only minor pro- LaMaskin, 2012). Major phases of arc mag- of sedimentary rocks imparts the full detrital portions of zircon grains from the other primary matism in the Jurassic and Early Cretaceous zircon age spectrum from the eroded strata to detrital zircon sources of North America (Fig. 4). occurred at 165–170 Ma and ca. 100 Ma in the subsequent deposit; therefore, comparison The Monteith A member is interpreted to the Omineca belt of interior British Columbia of detrital zircon spectra from older and younger have been derived principally from passive-mar- (Archibald et al., 1983). Late Cretaceous mag- sedimentary rocks is a valid means of detecting gin strata via transversely oriented rivers that matism is represented in the Idaho batholith, sedimentary recycling (Hadlari et al., 2015). As debouched directly from the incipient moun- the Shuswap complex of southeastern British a result, consideration of continentwide, pre- tain belt (Kukulski et al., 2013a; Raines et al., Columbia, and isolated areas of central British Jurassic sediment routing and recycling is criti- 2013). Recycling of Neoproterozoic to Ordovi- Columbia south of the Bowser Basin (Hyndman, cal for interpreting the provenance of detrital cian strata can account for the majority of zircon 1983; Armstrong, 1988; Carr, 1995). zircon grains in the study area. grains in the Monteith A member sample; the

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Passive Margin - Southeastern British Columbia (Gehrels and Pecha, 2014) Group 4: Paleozoic–Neoproterozoic– Dominated Spectrum Triassic Whitehorse Formation (n=196) This provenance group includes the Monte- Pennsylvanian Spray Lakes Group (n=198) ith C member, Monteith B member, and Falher A Member and is characterized by the relative importance of Paleozoic and Neoproterozoic Devonian Sassenach Formation (n=100) detrital zircon grains that are interpreted to be associated with the Appalachian orogen (285– Ordovician Mount Wilson 850 Ma; Fig. 4). This group is also characterized Formation (n=193) by relative importance of detrital zircons attrib- uted to the Grenville orogen over detrital zir- cons from the Trans-Hudson orogen (Fig. 6B). Cambrian Hamill Group (n=196) The Cretaceous Falher A Member has a higher proportion of Cordilleran zircon grains than the Neoproterozoic Horsethief Jurassic Monteith Formation samples in this Creek Group (n=195) group, indicating increased availability of Cor- dilleran arc detritus. Jurassic Eolianites, Southwestern United States (Dickinson and Gehrels, 2009; Leier Similar Paleozoic and Neoproterozoic detri- and Gehrels, 2011) tal zircon ages occur in Triassic passive-margin (N=10, n=942) strata of western North America and in eoli- anites in the southwestern United States (Fig. 5; Dickinson and Gehrels, 2009; Leier and Gehrels, 0 500 1000 1500 2000 2500 3000 2011; Gehrels and Pecha, 2014; Golding et al., Age (Ma) 2016). On the basis of a more complete data set Figure 5. Probability density plots of recycled zircon sources including passive- including paleoflow measurements and petrog- margin and Jurassic eolianites from western North America (Leier and Gehrels, raphy, the Monteith C and Monteith B members 2011; Gehrels and Pecha, 2014). were interpreted to have received significant contributions from basin-axial paleorivers with catchments including the southwestern United remainder could be derived from Devonian to through Ordovician strata (Fig. 5; Gehrels States and/or the Appalachian system directly Triassic strata, indicating that passive-margin and Pecha, 2014). The addition of Jurassic– (Fig. 5; Raines et al., 2013). An axial river strata were the primary sediment source for Cretaceous zircon grains indicates increased source is the favored interpretation for group this unit (Fig. 5; Gehrels and Pecha, 2014). The input from the magmatic arc (Armstrong, 1988). 4 based on various investigations (e.g., Ham- youngest mode (200 Ma) indicates that paleoriv- blin and Walker, 1979). This axial paleoriver ers with catchments extending westward to the Group 3: Proterozoic-Dominated system may have reactivated during deposition Cordilleran magmatic arc existed during deposi- Spectrum of the Falher A Member, which is consistent tion of the Monteith A member. with paleogeographic interpretations (Leckie This provenance group includes the most and Smith, 1992). Group 2: Yavapai-Mazatzal/Trans-Hudson– samples and is the most internally diverse. It Dominated Spectrum with Significant includes the Monteith C member (Raines et al., Group 5: Cordilleran Arc–Dominated Cordilleran Arc 2013), Gething Formation, Falher D Member, Spectrum Cadotte Member, Cardium Formation, and Chi- This provenance group includes samples nook Member (Fig. 6). These units are charac- This provenance group includes only the from the Cadomin Formation, Bluesky Forma- terized by a more equal representation of the Notikewin Member, where 75% of the ages in tion, and Dunvegan Formation (Fig. 6), which Proterozoic-age groups (i.e., Grenville, Gran- this sample were derived from the Cordillera are all components of distinct tectonostrati- ite-Rhyolite Province, Yavapai-Mazatzal, and (<252 Ma; Fig. 4). This is 52% more than the graphic wedges (Table 1; Fig. 3). These samples Trans-Hudson; Fig. 4). next nearest sample (Cardium Formation). are characterized by a dominant mode centered The samples in this group contain a wide The Notikewin Member is interpreted to have at ca. 1800 Ma. They all contain a significant spectrum of Proterozoic ages that are attributed derived from paleorivers with catchments that proportion of zircon grains attributed to the to recycling from passive-margin strata (Gehrels included the Cordilleran magmatic arc. Jurassic Yavapai-Mazatzal Province (1620–1790 Ma), as and Pecha, 2014). However, unlike groups 1 and detrital zircon grains (ca. 165 Ma) arrived in the well subordinate modes from every other major 2, the ca. 1800 Ma mode is subordinate. The basin as early as the Late Jurassic (Monteith C North American detrital zircon source. Group 2 proportions of different zircon populations are member), but they did not dominate until depo- is distinguished from group 1 by additional Cor- more similar to Devonian–Triassic strata of the sition of the Notikewin Member in the Albian. dilleran arc–derived zircon grains (Fig. 4). passive margin than to Neoproterozoic–Ordovi- Therefore, deposition of this member is likely This provenance group is interpreted to cian deposits (Fig. 5; Gehrels and Pecha, 2014). associated with a time of major Middle Jurassic derive, in large part, from passive-margin strata The presence of Mesozoic ages indicates incor- pluton unroofing. Plutons of this age are common of western North America. Like Group 1, these poration of the magmatic arc in the catchments in the Omineca belt of interior British Columbia sediments are very similar to Neoproterozoic of each unit. (Archibald et al., 1983; Armstrong, 1988).

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A 4. Paleozoic-Neoproterozoic dominated 5. Cordilleran arc dominated Monteith B mb. n=134 n=138

0123 Ga 0123Ga

Notikewin 3. Proterozoic dominated Gething Fm. n=132

0123Ga MonteithB 2. Yavapai-Mazatzal/Trans-Hudson MonteithC FalherA dominated, signi cant Cordilleran arc Chinook Bluesky Fm. Cadotte FalherD n=95 Cardium MonteithC Gething Raines et al. 0123 Cadomin Ga 1. Trans-Hudson dominated, Dunvegan Bluesky Legend minor Cordilleran arc Tectonic quiescence n=99 Tectonostratigraphic Wedge 3 MonteithA Tectonostratigraphic Wedge 2 Raines et al. Tectonostratigraphic Wedge 1 0123 B Ga 1850±50 Ma

Group 1

Group 2 160±50 Ma

Group 3 Group 5

Group 4

1050±50 Ma

600±50 Ma

Figure 6. (A) Multidimensional scaling plot of detrital zircon ages, highlighting five distinct provenance groups. One probability density plot from each provenance group is shown, illustrating the differences. The tectonostratigraphic wedge origin of each sample is indicated (Cant and Stockmal, 1989). (B) Multidimensional scaling plot with four synthetic age populations, also highlighting provenance groups.

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DISCUSSION High-Flux Episode DeCelles et al. (2009) hypothesized linkages Increased Depositional Slope between upper- and lower-plate processes. In and Sediment Flux to Basin their model, underthrusted retroarc crust melts and forms a dense eclogitic root that founders into the mantle. Following this foundering, a Uplift/Plateau period of increased magmatism occurs, termed Phase a high-flux episode (Fig. 7). This increase in Underthrusting magmatism is associated with plateau uplift and extension in the interior of the orogen, chang- Gravitational ing the taper angle of the orogenic wedge and Foundering of driving a period of shortening in the retroarc Eclogitic Root thrust belt as the plateau collapses and spreads laterally. A period of quiescence occurs when the taper of the orogenic wedge becomes sub- Figure 7. Sketch demonstrating processes behind high-flux mag­matic episodes. critical; subsequently, the crust is pulled down Foundering of the eclogitic root into the mantle causes plateau uplift and wide­ during the formation of the next eclogitic root spread magmatism.­ Uplift in the hinterland increases sedimentation in the (DeCelles et al., 2009). These processes should foreland (after De­Celles et al., 2009). be manifested in the fill of a foreland basin in four ways: (1) increased sediment supply during periods of uplift; (2) propagation of a flexural density plots of Cordilleran detrital zircon peaks number of zircon grains that can be analyzed wave creating basin subsidence during thrust from the foreland basin, the recurrence interval to produce a robust data set. Using the basin as loading; (3) evolving provenance from migrat- of these peaks (<50 m.y.) is not on the same a means to sample the arc is also advantageous ing drainage divides driven by cyclical uplift; scale as the supercontinent cycles investigated because detrital zircon grains in the basin were and (4) evolving provenance linked to evolv- by previous workers. derived from plutons and volcanic deposits that ing sediment routing systems (DeCelles et al., Compiling detrital zircon ages from the may have been completely eroded. 2009). The formation of unconformities is not basin is complementary to bedrock mapping Ar-Ar fault gouge cooling ages from the explicitly predicted in this model; however, we for understanding the magmatic history of the fold-and-thrust belt and K-Ar dates from plu- propose that periods between high-flux episodes Canadian Cordillera. The sedimentary system tons in the Kootenay arc of south-central British may be linked with times of uplift in the basin in is arguably a more efficient way of sampling Columbia are included with the detrital zircon response to denudation of thrust loads. the arc because river systems act as a random data and show a general temporal association We compiled detrital zircon ages younger sampling mechanism and concentrate a large with the episodic modes in the detrital zircon than 200 Ma from foreland basin strata of Alberta, Montana, and British Columbia (Fig. 8). A key interpretation is that prominent detrital zircon age modes for the basin correspond to Signi cant Unconformities major episodes of magmatism in the adjacent Mica K-Ar Cooling Age (Archibald et al., 1983) arc, which correspond to high-flux episodes Fault gouge cooling ages (Pana and van der Pluijm, 2015) (DeCelles et al., 2009; Laskowski et al., 2013). Mica K-Ar Thermal Overprinting Age (Archibald et al., 1983) There are three major modes in the probability density function at ca. 165, 115, and 74 Ma (Fig. 8). The proportion of zircon grains in each mode is interpreted as a bias toward sampling of older strata that predate the younger modes, and the Detrital Figure 8. Probability density function availability of the older detrital zircon grains of foreland basin detrital zircon ages Zircon Ages to young and old strata; therefore, the promi- younger than 200 Ma compiled from n=1193 nence of the modes does not represent inten- this study; Ross et al. (2005); Fuen- sity of an individual magmatic episode. Other tes et al. (2011); Leier and Gehrels factors that may contribute to bias are differ- (2011); Buechmann (2013); Raines et ences in zircon fertility (e.g., Dickinson, 2008), al. (2013); Benyon et al. (2014, 2016); and Blum and Pecha (2014). The depth of magma emplacement, and preserva- detrital zircon modes are interpreted tion bias (Hawkesworth et al., 2009; Spencer to represent the high-flux episodes et al., 2015b). Selective preservation of zircon of DeCelles et al. (2009). from the collisional phase of supercontinent cycles and preferential destruction from sub- duction and rifting phases have been described by Hawkesworth et al. (2009) and Spencer et al. (2015b). While preservation bias could poten- 50 100150 200250 tially explain episodic peaks in the probability Age (Ma)

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data (Fig. 8; Archibald et al., 1983; Pana and The second high-flux episode is proposed to Beaumont et al., 1993; Bhattacharya, 1994; Plint, van der Pluijm, 2015). This association indicates have occurred at ca. 115 Ma (Fig. 8). This is 2000; Collom, 2001; Shank and Plint, 2014; that the proposed high-flux episodes were peri- also associated with fault gouge dates overlap- Benham and Collom, 2012). Sediment supply ods of orogen denudation and thrusting in the ping the waning phase of apparent magmatic estimates are low for the Dunvegan, Cardium, retroarc. The durations of major unconformities activity (Pana and van der Pluijm, 2015). Fol- and Chinook units in comparison to the Fort are also plotted to highlight periods of uplift lowing this event, a major period of basin sub- St. John Group and Monteith Formation–Upper in the basin. With this framework of magmatic sidence and sedimentation occurred, associated Minnes Group (Stott, 1984). A possible explana- pulses, the provenance evolution of the stratigra- with deposition of the Spirit River Formation tion of these data is that periods between high- phy at Grande Cache and the subdivision of the (Leckie and Smith, 1992). Stott (1984) estimated flux episodes are predicted by the model to be stratigraphy into tectonostratigraphic packages that sedimentation rates increased during depo- characterized by mountain belts with less eleva- are given broader context. sition of the Fort St. John Group, based on bio- tion, possibly contributing to reduced sedimenta- The first major high-flux episode is proposed stratigraphic control and measured stratigraphic tion in the adjacent basin (DeCelles et al., 2009). to have occurred in the Canadian Cordillera at thicknesses. The provenance during this interval The Campanian magmatic event (ca. 74 Ma) ca. 165 Ma. According to fault gouge cooling evolved from a North American passive-margin– is more closely associated in time with Brazeau- ages, this high-flux episode was followed by a derived signature (i.e., Falher D Member), to one Paskapoo sedimentation of the Saunders Group period of thrusting as predicted by the model that likely represents axial input (i.e., Falher A (Figs. 1 and 3). This interval is dominated by (Fig. 8; DeCelles et al., 2009; Pana and van der Member), to a Mesozoic Cordilleran-dominated fluvial sediments and elevated sedimentation Pluijm, 2015). We interpret that uplift following signature (i.e., Notikewin Member; Fig. 4). The rates, although it does not outcrop in the vicinity the foundering of the crustal root led to increased preponderance of Cordilleran-derived Meso- of Grande Cache and is therefore not included in sediment supply and the infilling of the basin as zoic zircon grains in the Notikewin Member this study (Stott, 1984; Leckie and Smith, 1992). recorded by the first tectonostratigraphic wedge is attributed to denudation in the orogen suffi- The Saunders Group may represent the final (Fig. 1). The provenance during this time is inter- cient to unroof ca. 165 Ma plutons emplaced phase of high sediment input and basin filling preted to have evolved from basin-axial input in the Omineca belt during the first high-flux following the proposed Late Cretaceous high- rich in Appalachian detrital zircon grains recy- episode. The drainage divide is interpreted to flux episode. This package of sediment has been cled from the southwestern United States, cul- have migrated far to the west during deposition described as the thickest accumulation of sedi- minating in provenance dominated by recycled of the Notikewin Member. ment in the basin deposited during the time of zircon grains derived from passive-margin rocks The ca. 115 Ma mode is associated with maximum thrust shortening (Ross et al., 2005). to the west of the study area that were uplifted a subordinate mode at ca. 104 Ma potentially The analysis presented here understates the during this first episode of deformation (Figs. indicating that Aptian–Albian magmatic activity potential significance of terrane accretion events 4 and 6). This change reflects evolution from extended over a protracted time period (Fig. 8). in the Canadian Cordillera. Both terrane accre- an underfilled marine basin with low sediment The subordinate mode overlaps with the dura- tion events and high-flux episodes occurred input from the adjacent orogen to a basin domi- tion of the sub-Paddy unconformity (Stelck episodically, and each analysis has shortcom- nated by westerly derived sediment (Miles et al., and Leckie, 1990). This makes the association ings when comparing the timing of Cordilleran 2012). The transition from axial river systems between magmatic lulls and unconformities less events to the stratigraphic record (Figs. 1 and to transverse river systems in a foreland basin evident than in the case of the sub-Cretaceous 8; Price et al., 1981; Cant and Stockmal, 1989). has been attributed to decreased tectonic loading unconformity. The cyclical model is attractive because it and uplift in the orogen caused by erosion-driven The final phases of sedimentation in the study incorporates a more diverse suite of processes isostatic uplift (Burbank, 1992). This is consis- area are more difficult to link to the magmatic that are interpreted to operate in Cordilleran sys- tent with the interpreted provenance evolution flux proxy. The age of the last high-flux epi- tems (DeCelles et al., 2009). The cyclical model of the Montieth Formation (Raines et al., 2013). sode at ca. 74 Ma postdates the strata of this is also advantageous because the absolute ages of From 145 to 125 Ma, the sub-Cretaceous study. The Cadotte-Chinook interval could either magmatic events are more precisely constrained unconformity formed, attributed to basin uplift be related to a continuation of the second tec- than the timing of accretion events, allowing for as orogenic activity waned (Heller et al., 1988; tonostratigraphic wedge or a time of tectonic a more rigorous comparison of orogenic events Cant and Stockmal, 1989; Ross et al., 2005). The quiescence (cf. Cant and Stockmal, 1989; Pana and the preserved foreland stratigraphy (Price et sub-Cretaceous unconformity corresponds to a and van der Pluijm, 2015). The detrital zircon al., 1981; Cant and Stockmal, 1989). time of decreased magmatism inferred from the provenance of the Cadotte-Chinook interval The terrane accretion model allows for a rarity of zircon grains of this age in the foreland shows an evolution from broad, passive-margin more straightforward understanding of load basin (Fig. 8). This period of basin uplift transi- spectra to those increasingly dominated by Cor- emplacement and flexural response of the tioned into the deposition of the Bullhead Group, dilleran detritus. This pattern is similar to that lithosphere (Stockmal and Beaumont, 1987; which does not thicken abruptly westward and is of the second tectonostratigraphic wedge that Cant and Stockmal, 1989). Critiques of the ter- considered by some to record a period of erosion culminated in deposition of the Notikewin Mem- rane accretion model include: (1) mismatched and reworking, as opposed to a phase of high ber (Fig. 4). The cumulative stratigraphic thick- scales between accreted terranes and sediment subsidence and elevated sedimentation (Cant ness of the Codotte-Chinook interval is ~1200 volumes in the foreland; (2) the easterly trans- and Stockmal, 1989; Heller and Paola, 1989; m, indicating significant subsidence (Fig. 3). In mission of lithospheric stresses associated with Hayes et al., 1994). The provenance of the Cado- general, these units are characterized by shale- accretion events that occurred far outboard of min and Gething Formations is interpreted to be dominated sedimentation in the basin punctu- the foreland basin (i.e., the Bridge River ter- recycled passive-margin deposits, though the ated by progradational cycles of coarser deltaic rane, ~500 km; Coney et al., 1980); and (3) the basin-scale sediment routing system was char- and shoreface sediments (Lerand, 1983; Smith possibility of large strike-slip reorganization of acterized by axial river systems during this time et al., 1984; Walker, 1983; Rahmani and Smith, the orogenic collage (Cowan et al., 1997). These (Jackson, 1984; Hayes et al., 1994). 1988; Leckie, 1989; Leckie and Smith, 1992; issues necessitated the caveat that small and

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far outboard accretion events do not influence respectively. These sediments are separated Sedimentary Research, v. 84, p. 136–143, doi:10​ ​.2110​ /jsr​.2014​.16. basin subsidence directly but act as drivers of by an intervening unconformity (10–20 m.y.) Benyon, C., Leier, A.L., Leckie, D.A., Hubbard, S.M., and Geh- deformation toward the retroarc foreland basin, and magmatic lull that are interpreted as a time rels, G.E., 2016, Sandstone provenance and insights in therefore acting as a mechanism for deposition of basin uplift. The uppermost stratigraphy in the paleogeography of the McMurray Formation from detrital zircon geochronology, Athabasca Oil Sands, of tectonostratigraphic wedges (Stockmal and this study records a package of sediment that Canada: American Association of Petroleum Geolo- Beaumont, 1987; Cant and Stockmal, 1989; predates the last high-flux episode. Estimates gists Bulletin, v. 100, no. 2, p. 269–287, doi:​10​.1306​ Beaumont et al., 1993). This caveat may be of sedimentation rates suggest that these units /10191515029. Bhattacharya, J.P., 1994, Cretaceous Dunvegan Formation validated by observations in the northern North were deposited during a period of high subsid- of the Western Canada Sedimentary Basin, in Mossop, American Cordillera, where the Yakutat block ence and low sediment supply. The final high- G.D., and Shetsen, I., compilers, Geological Atlas of the is accreting to the Alaska margin and driving flux episode is linked to a particularly thick Western Canada Sedimentary Basin: Edmonton, Alberta, Canadian Society of Petroleum Geologists and Alberta shortening over 800 km away in the backarc stratigraphic succession of nonmarine deposits, Research Council, p. 365–373. (Mazzotti and Hyndman, 2002). There are no which was not an emphasis in this study. Black, L.P., Kamo, S.L., Allen, C.M., Davis, D.W., Aleinkoff, J.N., Valley, J.W., Mundil, R., Campbell, I.H., Korsch, R.J., Wil- data to suggest that this collision is contribut- This analysis shows the feasibility of link- liams, I.S., and Foudoulis, C., 2004, Improved 206Pb/238U ing significant sediment to the foreland basin. ing underplating, eclogitic root foundering, microprobe geochronology by the monitoring of trace- More detailed studies are needed to assess episodic magmatism and uplift, and collapse element–related matrix effects; SHRIMP, ID-TIMS, ELA- ICP-MS and oxygen isotope documentation for a series the relationship between terrane accretion of the orogen with foreland basin fill, inform- of zircon standards: Chemical Geology, v. 205, p. 115– events and other orogenic processes. The high- ing a more integrated understanding of cyclicity 140, doi:​10​.1016​/j​.chemgeo​.2004​.01​.003. flux episodes occurred during and in-between in Cordilleran orogenic systems. The cyclical Blum, M., and Pecha, M., 2014, Mid-Cretaceous to Paleocene North American drainage reorganization from detrital terrane accretion events, and there are more model presented here for the organization of zircons: Geology, v. 42, no. 7, p. 607–610, doi:​10​.1130​ terrane accretion events reported for the Cana- the foreland basin stratigraphy deemphasizes /G35513​.1. Buechmann, D.L., 2013, Provenance, Detrital Zircon U-Pb Geo- dian Cordillera than there are high-flux epi- the effect of terrane accretion as the key driver chronology and Tectonic Significance of Middle Creta- sodes (Figs. 1 and 8). Therefore, the argument of Alberta foreland basin deposition, although it ceous Sandstones from the Alberta foreland basin [Ph.D. that they are linked is problematic. This may is perhaps likely that the strata record a complex thesis]: Houston, Texas, University of Houston, 97 p. Burbank, D.W., 1992, Causes of recent Himalayan uplift de- necessitate favoring one model over the other, interplay between cyclical orogen development duced from depositional pattern in the Ganges basin: or constructing a hybrid model that integrates and sequential terrane accretion. Nature, v. 357, p. 680–683, doi:10​ .1038​ /357680a0.​ cyclical uplift and episodic terrane accretion to Cant, D.J., and Stockmal, G.S., 1989, The Alberta foreland basin: Relationship between stratigraphy and Cordil- ACKNOWLEDGMENTS more completely honor the stratigraphic record. leran terrane-accretion events: Canadian Journal of Funding for this research was generously provided by Shell Earth Sciences, v. 26, p. 1964–1975, doi:10​ .1139​ /e89​ -166.​ Canada (undergraduate thesis of R. van Drecht) and a Natu- Carr, S.D., 1995, The southern Omineca belt, British Colum- CONCLUSIONS ral Sciences and Engineering Research Council Discovery bia: New perspectives from the Lithoprobe Geoscience grant to S. Hubbard. Dale Leckie provided helpful discussions. Program: Canadian Journal of Earth Sciences, v. 32, The stratigraphy of the Alberta foreland Reviews by Christopher Spencer, Andrew Miall, and Science p. 1720–1739, doi:​10​.1139​/e95​-135. Editor Kurt Stüwe improved the clarity of the manuscript and Casas, I.E., and Walker, R.G., 1997, Sedimentology and depo- basin has been subdivided into tectonostrati- are greatly appreciated. sitional history of units C and D of the Falher Member, graphic wedges, which provide the context Spirit River Formation, west-central Alberta: Bulletin of for analysis of provenance evolution in Late REFERENCES CITED Canadian Petroleum Geology, v. 45, no. 2, p. 218–238. 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REVISED MANUSCRIPT RECEIVED 8 APRIL 2016 tion of the Cordilleran orogeny (southwestern Alberta, Stockmal, G.S., and Beaumont, C., 1987, Geodynamic mod- MANUSCRIPT ACCEPTED 21 APRIL 2016 Canada) inferred from detrital mineral geochronology, els of convergent margin tectonics: The southern Ca- geochemistry, and Nd isotopes in the foreland basin: nadian Cordillera and the Swill Alps, in Beaumont, C., Printed in the USA

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