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GEOSPHERE Detrital zircons and sediment dispersal in the Appalachian foreland

GEOSPHERE; v. 13, no. 6 William A. Thomas1, George E. Gehrels2, Stephen F. Greb3, Gregory C. Nadon4, Aaron M. Satkoski5, and Mariah C. Romero6 1Emeritus, University of Kentucky, and Geological Survey of Alabama, P. O. Box 869999, Tuscaloosa, Alabama 35486-6999, USA doi:10.1130/GES01525.1 2Department of Geosciences, University of Arizona, Tucson, Arizona 85721, USA 3Kentucky Geological Survey, University of Kentucky, Lexington, Kentucky 40506-0107, USA 4 12 figures; 3 supplemental files Department of Geological Sciences, Ohio University, Athens, Ohio 45701-2979, USA 5Department of Geoscience, University of Wisconsin, Madison, Wisconsin 53706-1692, USA 6Department of Earth, Atmospheric, and Planetary Sciences, Purdue University, West Lafayette, Indiana 47907, USA CORRESPONDENCE: geowat@uky.edu

CITATION: Thomas, W.A., Gehrels, G.E., Greb, S.F., Nadon, G.C., Satkoski, A.M., and Romero, M.C., 2017, Detrital zircons and sediment dispersal in the Appala ABSTRACT INTRODUCTION chian foreland: Geosphere, v. 13, no. 6, p. 2206–2230, doi:10.1130/GES01525.1. Seven new detrital-zircon U-Pb age analyses along with a compilation The late Paleozoic Appalachian orogen along eastern North America (Fig. 1) of previously published data from Mississippian–Permian sandstones in the long has been recognized as the dominant source of clastic sediment spread- Received 6 March 2017 Appalachian foreland (total n = 3564) define the provenance of Alleghanian ing cratonward into orogenic foreland basins (e.g., King, 1959; Thomas, 1977) Revision received 10 July 2017 Accepted 27 September 2017 synorogenic clastic wedges, as well as characterize the detritus available to and beyond, into intracratonic basins and farther across the North American Published online 19 October 2017 any more extensive intracontinental dispersal systems. The samples are from Midcontinent (e.g., Gehrels et al., 2011). The late Paleozoic orogen represents the cratonward-prograding Mauch Chunk–Pottsville clastic wedge centered the final assembly of supercontinent Pangaea as a result of a succession of on the Pennsylvania salient, the cratonward-prograding Pennington-Lee clas- Ordovician–Permian (Taconic, Acadian, and Alleghanian) accretionary pro- tic wedge centered on the Tennessee salient, and a southwestward-directed cesses along the Neoproterozoic–Cambrian Iapetan rifted margin of Lauren- longitudinal fluvial system along the distal part of the foreland. Grenville-age tia and the Cambrian–Ordovician passive margin (e.g., Hatcher et al., 1989a; detrital zircons generally are abundant in all samples; however, ages of Williams, 1995). The orogen includes the Precambrian Grenville province of the Taconic and Acadian orogenies are dominant in some samples but are supercontinent Rodinia assembly, synrift and passive-margin rocks of the minor to lacking in others. Taconic–Acadian ages are dominant in the Mauch Laurentian margin, and Ordovician through Permian synorogenic rocks and Chunk–Pottsville clastic wedge, in parts of the longitudinal system, and in accreted terranes of the Appalachian and Ouachita orogenic belts (Fig. 1). The the upper part (above Middle Pennsylvanian) of the Pennington-Lee clastic objectives of this article are to characterize the detrital-zircon populations of wedge; but they are minor to lacking in the lower part (Upper Mississippian– the late Paleozoic synorogenic clastic wedges within the Appalachian foreland Lower Pennsylvanian) of the Pennington-Lee clastic wedge. New Hf isotopic and to evaluate the contributions of the various components of the prove- analyses show a similar distinction between the two clastic wedges, sup- nance within the Appalachian orogen. This characterization of Appalachian porting an interpretation of differences in provenance contributions during detrital-zircon populations provides a template to determine possible Appala- the early stages of basin filling. U-Pb ages and Hf isotopic ratios also indicate chian contributions to more distal intracontinental dispersal systems. that the Mauch Chunk–Pottsville transverse dispersal fed the northern part of the longitudinal system. A few samples in the distal southwestern part of LATE PALEOZOIC SYNOROGENIC SEDIMENTARY DEPOSITS the Mauch Chunk–Pottsville clastic wedge and adjacent parts of the longitudinal system have unusually large populations of grains with Superior and Mississippian–Permian Alleghanian synorogenic clastic deposits vary sig- Central Plains ages. The relative distance and isolation of these samples from nificantly along the orogen. Between the New York and Alabama promontories, the Canadian Shield, which is the primary source of Superior and Central two late Paleozoic classic synorogenic clastic wedges filled foreland basins cen- Plains zircons, indicates likely recycling from synrift sediment, passive-mar- tered on the Pennsylvania and Tennessee embayments (Fig. 2). From the New gin strata, or Taconic–Acadian clastic wedges. Among the lesser components York promontory northward to Newfoundland, late Paleozoic clastic sedimenta- are a few grains with ages that correspond to Iapetan synrift igneous rocks tion along the Appalachian orogen filled fault-bounded pull-apart basins along and also to Pan-African–Brasiliano components of Gondwanan accreted ter- a regional system of dextral strike-slip faults (Fig. 1) (e.g., Thomas and Schenk, For permission to copy, contact Copyright ranes. Synorogenic zircons of the Alleghanian orogeny are very rare (seven 1988; van de Poll, 1995). From the Alabama promontory westward along the Permissions, GSA, or [email protected]. grains in the total of 3564). Ouachita and Marathon embayments, late Paleozoic synorogenic clastic wedges

90W 80W 70W 60W Newfoundland50N EXPLANATION embaymen Appalachian-Ouachita thrust front t Appalachian basement (Grenville) massifs

outline of Ouachita late Paleozoic clastic wedges Ganderia faults within late Paleozoic Maritimes basin 55W boundaries of Gondwanan accreted terranes Avalonia 50N SUPERIOR GRENVILLE 45N outline of Acadian clastic wedge St. Lawrence outline of Taconic clastic wedges promontory

maximum thickness in Taconic clastic wedges

transformIapetan rifted margin of Laurentia M.R. Meguma Quebec (palinspastic location) Ganderia embaymen

rift t synrift intracratonic basement faults 45N GRENVILLE FRONT 60W PENOKEAN 65W 100W 95W 40N

105W CENTRAL New 40N Yo PLAINS promontoryrk GRANITE- Pennsylvania RHYOLITE embaymen t B.R. 70W

nia Virginia 35N 35N promontory Caroli Tennessee embayment

Ouachit 75W embaymen 80W GRENVILLE FRONT Suwannee a Figure 1. Regional map of potential provenance elements in the Appalachian orogen in eastern 30N 30N North America: Precambrian provinces of the craton (modified from Van Schmus et al., 1993); Alabama Iapetan rift margin and synrift intracratonic faults of Laurentia, which outline the locations of 105W t promontory synrift igneous and sedimentary rocks, as well as the approximate trace of the passive-margin shelf edge (from Thomas, 2014); generalized outlines of Taconic and Acadian synorogenic clastic Marathon wedges (from Thomas, 1977, and references therein); boundaries of Gondwanan accreted terranes Texas (from Hibbard et al., 2007; Hatcher, 2010); trace of the Appalachian-Ouachita thrust front (compiled embaymen promontory 90W 85W from Thomas et al., 1989b; Hatcher, 2010); basement massifs of Grenville-age rocks (from Hatcher, N 2010); locations of faults within the late Paleozoic Maritimes basin in the northern Appalachians (from Thomas and Schenk, 1988; van de Poll, 1995); and outline of late Paleozoic clastic wedges t 0 200 400 600 km along the Ouachita orogen (from Thomas, 2006). Gray outline shows the location of the map in 100W 95W Figure 2. B.R.—Blue Ridge external basement massif; M.R.—Midcontinent rift system.

Mauch Chunk–Pottsville clastic wedge A PA B NW SE e 3 16 Md Penn 16 Sharp Mtn. Figure 2. (A) Map of sample sites in the 13 3 Sharon-N 13 Tumbling Run context of directions of progradation of e Lw Penn 4 Sharon-S clastic sediment within the Mauch Chunk– 14 Pottsville (blue arrows) and Pennington- OH 7 1 Up Miss 21 Mauch Chunk–Pottsville clastic wedge Lee (red arrows) clastic wedges, as well 17-19 WV SW NE 20 clastic wedg as the Early Pennsylvanian longitudinal 4 dispersal system (green arrow). Numbers Mauch Chunk–Pottsvill Lw Penn 14 Pottsville in circles indicate new analyses reported 4 Bluestone 1 Mauch Chunk in Supplemental Table S1 and plotted in KY 11 Up Miss 3 Princeton 2 Hinton Figure 3; numbers in rectangles indicate 6 7 10 2-4 1 Stony Gap 9 published analyses (references cited in 2 1 5 VA Fig. 4 provide analytical data, location, and Pennington-Lee clastic wedge longitudinal system 6 N stratigraphic information for each sample). TN 15 The location of this map is shown by out- 7 Proctor 21 Greene Lw Perm 20 Washington S line in Figure 1. The blue barbed line shows 8 19 upper Monongahela the Appalachian thrust front (from Fig. 1). Up Penn 18 lower Monongahela PA—Pennsylvania; OH—Ohio; WV—West AL Pennington-Leeclastic wedge 5 GA 17 Conemaugh Virginia; KY—Kentucky; VA—Virginia; TN— Md Penn Tennessee; AL—Alabama; GA—Georgia. 12 7 upper Raleigh (B) Diagrammatic cross sections (not to N Lw Penn 11 lower Raleigh 10 Bottom Creek scale) to show the stratigraphic position local 9 Pocahontas of sample sites (cross sections are approxi source Pennington-Lee clastic wedge 200 km mately along each of the blue and red NW SE Up Miss arrows in A). Numbers are the same as EXPLANATION OF SYMBOLS FOR SAMPLE LOCATIONS Md Penn 6 Princess #7 in A; color fills and outlines of numbered 1 KY-21-SG Stony Gap 5 Grundy-Norton circles and rectangles match those of the 2 KY-18-CB Corbin 2 Corbin Lw Penn 6 Lee arrows in A. Perm—Permian; Penn—Penn 23 OH-4-SN Sharon (north) Pennington-Lee clastic wedge sylvanian; Miss—Mississippian; Up— 4 OH-1-SS Sharon (south) SW NE Upper; Md—Middle; Lw—Lower. 5 VA-1-GN Grundy-Norton 15 6 KY-19-PR7 Princess No. 7 coal Md Penn Cross Mountain 7 WV-1-PR Proctor 12 Montevallo 8 Sewanee 6 previously published, listed by number in Figure 4 Lw Penn (local source) 5 Raccoon Mountain

of deep-water turbidites (Fig. 1) have relatively small wavelength-to-amplitude are more quartzose (Becker et al., 2005; Grimm et al., 2013). On the basis of ratios (Arbenz, 1989; Viele and Thomas, 1989). The shallow-marine to deltaic paleocurrents and sandstone petrography, the relatively lithic sandstones of clastic wedges in the Pennsylvania and Tennessee embayments have large the transverse drainage systems generally have been interpreted as being wavelength-to-amplitude ratios; these clastic wedges are the focus of this article. derived from unroofing of the internal belts of the Appalachian orogen south- The Mauch Chunk–Pottsville clastic wedge is centered on the Pennsylvania east of the foreland basins (Thomas, 1966; Meckel, 1967; Davis and Ehrlich, salient of the Appalachian thrust belt (Pennsylvania embayment of the rifted 1974; Edmunds et al., 1979; Donaldson and Shumaker, 1981; Donaldson et al., margin), and the Pennington-Lee clastic wedge is centered on the Tennessee 1985). Quartz pebbles are common in Lower Pennsylvanian polymictic con- salient of the thrust belt (Tennessee embayment of the rifted margin) (Figs. glomerates. In Pennsylvania, a southeastward increase in quartz-pebble sizes 1, 2) (Thomas, in Hatcher et al., 1989b). Sediment-dispersal patterns in both indicates a source along the southeast side of the foreland basin in the Penn- clastic wedges reflect generally semi-radial transverse drainages across the sylvania embayment (Meckel, 1967). In contrast, on the basis of paleocur- foreland basins toward the craton (Fig. 2) (e.g., Meckel, 1967; Thomas, 1977). In rents, as well as more quartzose composition and concentrations of quartz contrast to the transverse drainages, south- to southwest-directed longitudinal pebbles, Lower Pennsylvanian sandstones in the longitudinal drainage sys- (orogen-parallel) drainage characterized the distal parts of the basins in the tem have been interpreted as derived from the Canadian Shield or northern Early Pennsylvanian (Fig. 2) (Archer and Greb, 1995; Grimm et al., 2013). Appalachians (Siever and Potter, 1956; Edmunds et al., 1979; Chesnut, 1994; Sandstones of the transverse drainage systems in the proximal parts of Archer and Greb, 1995; Greb and Chesnut, 1996; Grimm et al., 2013), as has the clastic wedges generally are more lithic, whereas those of the Early Penn- one sandstone in the proximal part of the Mauch Chunk–Pottsville clastic sylvanian longitudinal drainage system along the distal parts of the basins wedge (Robinson and Prave, 1995).

Table S1. Zircon U-Pb geochronologic analyses by laser ablation–multicollector–inductively coupled plasma mass spectrometry: Mississippian–Permian sandstones Isotope ratios Apparent ages (Ma) DETRITAL-ZIRCON SAMPLING AND ANALYTICAL METHODS 232, and 238 were measured with Faraday detectors, whereas the smaller 202 Analysis U206Pb U/Th 206Pb* ±207Pb*±206Pb* ±error 206Pb*±207Pb*±206Pb* ±Best age± Conc (ppm)204Pb 207Pb* (% 2s) 235U* (% 2s) 238U (% 2s) corr. 238U* (Ma 2s) 235U (Ma 2s) 207Pb* (Ma 2s) (Ma) (Ma 2s) (%)

KY-21-SG—Stony Gap Sandstone Member—37° 09' 26.1'' N, 82° 38' 15.2'' W KY-21-SG-Spot 103676 88161 2.017.6102 2.00.46542.8 0.0594 1.90.70372.27.0 388.08.9 483.243.9 372.2 7.0 77.0 and 204 ion beams were measured with ion counters. The acquisition routine KY-21-SG-Spot 35 4471480492.0 18.1556 2.00.45642.5 0.0601 1.50.60376.25.5 381.77.9 415.444.1 376.2 5.5 90.6 KY-21-SG-Spot 1934371000.8 19.1888 5.50.43395.8 0.0604 1.80.31378.06.5 366.017.7290.4 125.6 378.0 6.5 130.2 KY-21-SG-Spot 79 24171415 1.317.9428 2.30.46482.9 0.0605 1.70.60378.66.4 387.69.3 441.751.7 378.6 6.4 85.7 KY-21-SG-Spot 277163 25517 2.218.1351 2.00.46442.8 0.0611 2.00.69382.27.3 387.39.2 418.045.7 382.2 7.3 91.4 KY-21-SG-Spot 7408 84208 0.817.8407 1.50.47992.0 0.0621 1.30.66388.35.0 398.06.6 454.433.8 388.3 5.0 85.5 KY-21-SG-Spot 26 12211785 1.518.5871 2.90.46843.4 0.0631 1.80.52394.76.8 390.111.0362.7 65.3 394.7 6.8 108.8 To document dispersal of detritus from the Appalachian orogen, samples included a 15 s integration on peaks with the laser off (for backgrounds), fif- KY-21-SG-Spot 56 44 19949 1.517.6004 5.60.49886.2 0.0637 2.70.43397.910.2410.9 20.9 484.5 123.6 397.9 10.2 82.1 KY-21-SG-Spot 24 1561670321.3 17.5105 2.70.51043.5 0.0648 2.20.62404.98.6 418.712.0495.7 60.3 404.9 8.6 81.7 KY-21-SG-Spot 22 16235662 2.117.5379 2.70.52583.2 0.0669 1.80.57417.37.4 429.011.3492.3 58.9 417.3 7.4 84.8 KY-21-SG-Spot 185264 81142 1.117.7310 1.90.52152.6 0.0671 1.70.67418.57.0 426.29.0 468.142.9 418.5 7.0 89.4 KY-21-SG-Spot 58 52 10205 1.417.7360 5.00.52275.8 0.0672 2.90.50419.511.8427.0 20.3 467.5 111.5 419.5 11.8 89.7 have been collected and analyzed through the stratigraphic succession of the teen 1 s integrations with the laser firing, and a 30 s delay to ensure that the KY-21-SG-Spot 230294 80181 1.117.7287 1.90.52512.9 0.0675 2.30.77421.29.3 428.510.3468.4 41.3 421.2 9.3 89.9 KY-21-SG-Spot 1378161193 1.116.7145 3.60.55784.0 0.0676 1.80.44421.87.2 450.114.7597.4 78.8 421.8 7.2 70.6 KY-21-SG-Spot 220265 30219 1.017.7848 1.90.52733.0 0.0680 2.30.77424.29.5 430.010.4461.4 41.9 424.2 9.5 91.9 KY-21-SG-Spot 157171 18993 1.118.2855 4.60.51375.0 0.0681 1.90.38424.97.8 420.917.1399.5 102.9 424.9 7.8 106.4 KY-21-SG-Spot 242431 1127902.8 18.1613 1.60.51762.3 0.0682 1.70.72425.26.9 423.68.0 414.735.7 425.2 6.9 102.5 KY-21-SG-Spot 256534 1174176.5 18.1809 1.60.51881.9 0.0684 1.10.57426.64.6 424.36.8 412.335.7 426.6 4.6 103.5 Mississippian–Permian synorogenic clastic wedges in the Appalachian basin previous sample was completely purged from the system. Smaller grains were KY-21-SG-Spot 314109 57739 1.417.6773 3.80.53464.1 0.0685 1.60.40427.36.8 434.814.6474.8 84.1 427.3 6.8 90.0 KY-21-SG-Spot 2407114232 0.917.8022 2.60.53484.5 0.0690 3.60.82430.415.2435.0 15.8 459.256.8 430.4 15.2 93.7 KY-21-SG-Spot 33 12581189 1.217.8438 3.10.53543.5 0.0693 1.60.44431.96.5 435.412.4454.0 69.7 431.9 6.5 95.1 KY-21-SG-Spot 183111 26320 2.118.0037 2.90.53173.9 0.0694 2.60.68432.711.1433.0 13.7 434.263.5 432.7 11.1 99.7 KY-21-SG-Spot 278119 1552981.4 17.6724 3.80.54324.3 0.0696 2.10.49433.98.9 440.615.4475.4 83.1 433.9 8.9 91.3 (Fig. 2). The new analyses include U-Pb ages and Hf isotopic data (Fig. 3) from analyzed with all Pb isotopes in ion counters, using a 20 μm beam diameter. KY-21-SG-Spot 2413045042.0 19.2836 5.50.51566.0 0.0721 2.40.39448.910.3422.2 20.8 279.2 127.0 448.9 10.3 160.8 KY-21-SG-Spot 215225 31093 1.017.6081 2.50.56743.0 0.0725 1.60.53451.06.9 456.310.9483.5 55.6 451.0 6.9 93.3 KY-21-SG-Spot 313147 2225162.0 17.9983 2.60.56083.7 0.0732 2.50.69455.411.2452.0 13.3 434.858.6 455.4 11.2 104.7 KY-21-SG-Spot 306167 62469 1.117.7560 2.80.56903.6 0.0733 2.20.62455.99.8 457.413.1465.0 62.0 455.9 9.8 98.0 KY-21-SG-Spot 284144 25841 2.717.3470 2.10.58252.9 0.0733 1.90.66455.98.3 466.110.7516.3 47.2 455.9 8.3 88.3 KY-21-SG-Spot 266129 46055 1.418.0727 3.10.56033.7 0.0734 2.00.54456.98.7 451.713.4425.6 68.7 456.9 8.7 107.4 detrital-zircon grains. In addition, previously published data for U-Pb ages of Analyses consisted of a 12 s integration on peaks with the laser off (for back- KY-21-SG-Spot 1154898702.4 16.9907 5.20.59855.8 0.0738 2.60.44458.711.3476.3 22.1 561.8 113.6 458.7 11.3 81.6 KY-21-SG-Spot 232159 67940 1.517.6434 3.00.57993.6 0.0742 2.10.57461.59.3 464.413.6479.0 66.2 461.5 9.3 96.3 KY-21-SG-Spot 188158 27209 1.817.0082 2.20.60202.8 0.0743 1.80.64461.88.0 478.510.8559.5 47.2 461.8 8.0 82.5 KY-21-SG-Spot 2518224077 1.717.9571 4.90.57255.3 0.0746 2.00.38463.69.0 459.619.6439.9 109.2 463.6 9.0 105.4 KY-21-SG-Spot 88 2721137371.9 16.7507 2.20.61972.6 0.0753 1.50.56468.06.7 489.710.2592.7 47.3 468.0 6.7 79.0 detrital zircons are available for comparison (Fig. 4). The data presentation in grounds), twelve 1 s integrations with the laser firing, and a 30 s delay to purge KY-21-SG-Spot 211146 29049 1.917.1054 2.00.61152.7 0.0759 1.90.69471.38.4 484.510.4547.1 43.1 471.3 8.4 86.1 KY-21-SG-Spot 50 3221526070.9 17.2672 2.10.60962.8 0.0763 1.70.63474.37.9 483.310.6526.5 47.1 474.3 7.9 90.1 KY-21-SG-Spot 1118911320 1.617.6969 3.20.67083.7 0.0861 1.80.50532.49.4 521.215.0472.3 70.7 532.4 9.4 112.7 KY-21-SG-Spot 246155 25768 1.216.4608 2.00.74222.9 0.0886 2.10.72547.311.2563.7 12.7 630.443.8 547.3 11.2 86.8 KY-21-SG-Spot 141290 80551 2.316.6937 1.80.75442.5 0.0913 1.80.71563.59.8 570.811.1600.0 38.4 563.5 9.8 93.9 KY-21-SG-Spot 46 94 38904 1.516.3000 2.90.82643.2 0.0977 1.40.42600.97.8 611.614.9651.5 63.0 600.9 7.8 92.2 Figures 3 and 4 is organized by depositional age to establish a time frame for the previous sample. evolution of drainage systems, as well as by distribution separately for trans- An average of 275 analyses was conducted on each sample with one U-Pb 1Supplemental Table S1. Zircon U-Pb geochronologic analyses by laser ablation–multicollector–inductively verse dispersal into the two clastic wedges and the longitudinal system in the measurement per grain. Grains were selected in random fashion; crystals were coupled plasma mass spectrometry: Mississippian– distal part of the basin. rejected only if they contained cracks or inclusions or were too small to be Permian sandstones. Please visit http://doi.org/10 analyzed. The use of high-resolution BSE and CL images provided assistance .1130/GES01525.S1 or the full-text article on www .gsapubs.org to view the Supplemental Table. in grain selection and spot placement. Sample Collection and Processing Data reduction was accomplished using the “agecalc” Microsoft Excel spreadsheet, which is the standard Arizona LaserChron Center reduction Approximately 12 kg of medium- to coarse-grained sandstone was col- protocol (Gehrels et al., 2008; Gehrels and Pecha, 2014). Data were filtered for lected from a restricted stratigraphic interval for each detrital-zircon sample discordance, 206Pb/238U precision, and 206Pb/207Pb precision as indicated in the and then processed utilizing methods outlined by Gehrels (2000), Gehrels et al. notes in Supplemental Table S1 (see footnote 1). Data are presented on nor- (2008), and Gehrels and Pecha (2014). Zircon grains were extracted using tra- malized age-probability diagrams (Fig. 3), which sum all relevant analyses and ditional methods of jaw crushing and pulverizing, followed by density sepa- uncertainties and divide each curve by the number of analyses such that all ration using a Wifely table. The resulting heavy-mineral fraction was further curves contain the same area. Age groups are characterized by the ages of purified using a Frantz LB-1 magnetic barrier separator and heavy liquids. A peaks in age probability and by the range of constituent ages. representative split of the zircon yield was incorporated into a 2.5-cm epoxy mount along with multiple fragments of the U-Pb primary standard Sri Lanka SL-F and Hf standards R33, Mud Tank, FC-1, Plesovice, Temora, and 91500. Hf Isotopic Analysis The mounts were sanded down to ~20 μm, polished to 1 μm, and imaged by back-scattered electrons (BSE) and cathodoluminescence (CL) using a Hitachi Hafnium isotopic analyses were conducted utilizing the Nu multicollector 3400N scanning electron microscope (SEM) and a Gatan Chroma CL2 detec- LA-ICPMS system at the Arizona LaserChron Center following methods re- tor system at the Arizona LaserChron SEM Facility (www.geoarizonasem.org). ported in Cecil et al. (2011) and Gehrels and Pecha (2014). An average of 45 Hf Prior to isotopic analysis, mounts were cleaned in an ultrasonic bath of 1% analyses was conducted per sample; grains were selected to represent each of HNO and 1% HCl in order to remove surficial common Pb. 3 the main age groups and to avoid crystals with discordant or imprecise ages.

Table S2: Hf isotopic data: Mississippian–Permian sandstones Order Sample (176Yb + 176Lu) / 176Hf (%) Volts Hf 176Hf/177Hf ± (1σ) 176Lu/177Hf 176Hf/177Hf (T) E-Hf (0) E-Hf (0) ± (1σ) E-Hf (T)Age (Ma) CL images were utilized to ensure that all Hf analyses are within the same KY-18-CB-27 4.72.1 0.282762 0.000072 0.000293 0.282760 -0.8 2.69.1 447 KY-18-CB-151 34.4 2.50.2824820.000040 0.002112 0.282465 -10.71.4 -1.7 431 KY-18-CB-155 20.1 2.50.2828220.000073 0.001552 0.282810 1.32.6 10.4 429 KY-18-CB-67 15.6 3.30.2821990.000031 0.001057 0.282190 -20.71.1 -10.8462 U-Pb Geochronologic Analysis domain as the U-Pb pit, although in most analyses Hf laser pits were located KY-18-CB-66 19.4 3.40.2821540.000034 0.001217 0.282125 -22.31.2 4.91255 KY-18-CB-69 7.73.7 0.281938 0.000048 0.000475 0.281923 -30.01.7 6.51639 KY-18-CB-68 7.23.9 0.281328 0.000044 0.000467 0.281305 -51.51.6 6.02567 KY-18-CB-156 15.0 2.70.2820250.000051 0.000888 0.281995 -26.91.8 11.8 1761 directly on top of the U-Pb analysis pits. Complete Hf isotopic data and Hf KY-18-CB-158 6.02.8 0.281061 0.000031 0.000387 0.281041 -61.01.1 -0.1 2708 KY-18-CB-159 18.1 2.90.2819800.000034 0.001193 0.281942 -28.51.2 7.91674 KY-18-CB-14 15.3 3.00.2812140.000037 0.000917 0.281166 -55.61.3 4.82724 2 KY-18-CB-13 19.9 2.60.2819300.000040 0.001316 0.281887 -30.21.4 7.51738 Uranium-lead geochronology of individual zircon crystals was conducted evolution plots of individual samples are presented in Supplemental Table S2 . KY-18-CB-12 6.52.4 0.282505 0.000034 0.000389 0.282501 -9.9 1.23.6 611 KY-18-CB-45 23.8 3.10.2809730.000036 0.001399 0.280893 -64.11.3 1.73007 KY-18-CB-44 10.6 2.90.2817240.000034 0.000643 0.281703 -37.51.2 2.01785 KY-18-CB-41 27.8 3.00.2822950.000039 0.001613 0.282260 -17.31.4 7.81174 by laser ablation–inductively coupled plasma mass spectrometry (LA-ICPMS) Hafnium data are presented using Hf evolution diagrams (Fig. 3), where KY-18-CB-56 9.93.1 0.282297 0.000025 0.000586 0.282285 -17.30.9 6.61085 KY-18-CB-57 14.3 3.20.2823150.000035 0.000881 0.282296 -16.61.2 7.21091 KY-18-CB-58 6.43.9 0.280953 0.000025 0.000404 0.280932 -64.80.9 -3.6 2724 176 177 KY-18-CB-59 16.8 2.30.2823330.000041 0.001020 0.282309 -16.01.4 11.9 1277 at the Arizona LaserChron Center (www.laserchron.org). The isotopic analyses initial Hf/ Hf ratios are expressed in εHft notation, which represents the Hf KY-18-CB-168 25.4 2.60.2820730.000034 0.001533 0.282037 -25.21.2 1.41241 KY-18-CB-167 13.1 3.20.2824120.000036 0.000727 0.282397 -13.21.3 11.3 1113 KY-18-CB-166 12.5 5.60.2826540.000026 0.000849 0.282646 -4.6 0.95.9 485 KY-18-CB-53 38.6 5.00.2821000.000037 0.002292 0.282035 -24.21.3 7.31503 involved ablation of zircon using a Photon Machines Analyte G2 excimer laser isotopic composition at the time of zircon crystallization relative to the chon- KY-18-CB-133 11.4 3.40.2826560.000049 0.000830 0.282649 -4.6 1.85.3 453 KY-18-CB-134 10.7 5.40.2821350.000027 0.000627 0.282119 -23.00.9 7.81393 KY-18-CB-31 9.85.5 0.280886 0.000035 0.000629 0.280854 -67.11.2 -6.5 2718 KY-18-CB-34 9.84.6 0.282311 0.000025 0.000621 0.282299 -16.80.9 6.01032 (λ = 193 nm) coupled to either a Nu Instruments multicollector ICPMS or a dritic uniform reservoir (CHUR) (Bouvier et al., 2008). Internal precision for KY-18-CB-35 12.7 4.50.2822830.000022 0.000756 0.282267 -17.70.8 6.71114 KY-18-CB-76 20.7 3.10.2823730.000039 0.001224 0.282349 -14.61.4 7.31012 KY-18-CB-157 26.8 4.40.2821570.000028 0.001681 0.282142 -22.21.0 -12.3468 176 177 KY-18-CB-102 4.74.6 0.282321 0.000023 0.000280 0.282318 -16.40.8 -6.3 458 Thermo Element2 single-collector ICPMS. Ultra-pure helium carried the ab- Hf/ Hf and εHft is reported for each analysis on Hf evolution plots in Sup- KY-18-CB-105 17.3 4.90.2821200.000034 0.001031 0.282093 -23.51.2 6.61380 KY-18-CB-118 10.6 4.10.2819690.000027 0.000679 0.281949 -28.91.0 4.21498 KY-18-CB-116 12.6 3.30.2822450.000043 0.000767 0.282228 -19.11.5 6.31160 KY-18-CB-256 29.1 4.80.2823610.000027 0.001664 0.282325 -15.00.9 9.81161 lated material from the HelEx cell into the plasma source of the ICPMS. plemental Table S2 (see footnote 2) and as the average for all analyses (2.4 KY-18-CB-355 9.63.8 0.282116 0.000040 0.000611 0.282099 -23.71.4 9.61504 KY-18-CB-221 20.2 2.90.2824580.000036 0.001263 0.282447 -11.61.3 -2.0 445 KY-18-CB-225 13.9 1.60.2818370.000042 0.000883 0.281810 -33.51.5 2.61648 KY-18-CB-222 13.3 3.40.2820790.000035 0.000810 0.282056 -25.01.2 7.71488 Analyses conducted with the Nu ICPMS utilized Faraday collectors for mea- epsilon units at 2σ) on Figure 3. On the basis of the in-run analysis of zircon KY-18-CB-223 8.53.6 0.282257 0.000037 0.000483 0.282247 -18.71.3 4.31041 KY-18-CB-206 6.86.3 0.281063 0.000028 0.000398 0.281042 -60.91.0 -0.2 2702 KY-18-CB-207 11.1 5.00.2824170.000035 0.000709 0.282403 -13.01.2 10.3 1064 238 232 208 KY-18-CB-208 10.3 5.30.2822600.000030 0.000686 0.282254 -18.61.1 -8.5 462 surement of U and Th, either Faraday collectors or ion counters for Pb, standards, the external precision is 2–2.5 epsilon units (2σ). Hf isotopic evo- KY-18-CB-201 14.2 4.20.2822130.000026 0.000845 0.282195 -20.20.9 3.61091 207 206 204 204 202 Pb, and Pb, and ion counters for Pb, Hg, and Hg (see Supplemental lution of typical continental crust is shown with arrows on εHft evolution dia- 2Supplemental Table S2. Hf isotopic data: Mississip- Table S11 for specific methods used for each sample), depending on grain size. grams, which are based on a 176Lu/177Hf ratio of 0.0115 (Vervoort and Patchett, pian–Permian sandstones. Please visit http://doi.org /10.1130/GES01525 .S2 or the full-text article on www For larger grains, a 30-μm-diameter spot was used, and masses 206, 207, 208, 1996; Vervoort et al., 1999). .gsapubs.org to view the Supplemental Table.

10 Figure 3. Relative U-Pb age-probability plots (lower panel) and Hf evolution dia DM gram (upper panel) showing results from analyses of Mississippian–Permian 5 sandstones in the Appalachian foreland (analytical data and location informa- 0 tion are in Supplemental Tables S1 [see CHUR footnote 1] and S2 [see footnote 2]). Lower panel: Relative age-probability plots for seven analyzed samples. Vertical –5 colored bands represent the age ranges of potential provenance provinces in the crustal Appalachians and North American craton. –10 evolution The plots are color coded as in Figure 2: blue—Mauch Chunk–Pottsville clastic Appalachians wedge; red—Pennington-Lee clastic wedge;

–15 ft Gander/Avalon green—longitudinal dispersal system.

& Grenville Upper panel: εHft data for six samples (data points are color coded and shown e

e- Granite-Rhyolite

–20 ville by symbols that are explained in the lower Superior Central Plains ntral Plains yolit cadian n-African– ans-Amazonian panel). The average uncertainty of Hf iso- ans-Hudson enokean & A Alleghanian Superior & Penokean Eburnian Tr Gren Ce Granit Rh P Tr Pa Brasiliano & Iapetan synri topic analyses (2.6 epsilon units at 2σ) is –25 shown in the upper right. The Hf evolution diagram shows the Hf isotopic composi-

conic tion at the time of zircon crystallization,

Ta Lower Permian Pennington-Lee clastic wedge in epsilon units, relative to the chondritic 7. WV-1-PR Proctor (n=234) uniform reservoir (CHUR) (Bouvier et al., 2008) and to the depleted mantle (DM) Middle Pennsylvanian Pennington-Lee clastic wedge (Vervoort and Blichert-Toft, 1999). Shown 6. KY-19-PR7 Princess No. 7 coal (n=284) for reference is the evolution of typical continental crust (black arrow), which is based on a 176Lu/177Hf ratio of 0.0115 Lower Pennsylvanian Pennington-Lee clastic wedge (Vervoort and Patchett, 1996; Vervoort et al., 1999). Reference fields, which are 5. VA-1-GN Grundy-Norton (n=274) shown by colored areas (explanation in lower right of upper panel), summarize Lower Pennsylvanian longitudinal system published Hf isotopic data for the Appa 3. OH-4-SN Sharon (north) (n=319) lachians (from Appalachian-derived detrital grains; Mueller et al., 2007, 2008), the Gander and Avalon accreted terranes (Willner et al., 2013, 2014; Pollock et al., 2015; Henderson et al., 2015), the Grenville orogen (Bickford et al., 2010; Gehrels and Pecha, 2014), Mesoprotero zoic rocks of

Normalized Probability Lower Pennsylvanian longitudinal system 4. OH-1-SS Sharon (south) (n=183) the Granite-Rhyolite province and Paleo proterozoic rocks of the Central Plains oro- Lower Pennsylvanian longitudinal system gen (Goodge and Vervoort, 2006; Bickford 2. KY-18-CB Corbin (n=319) et al., 2008; Gehrels and Pecha, 2014), and the Penokean and Superior provinces of the Canadian Shield (Gehrels and Pecha, 2014). Upper Mississippian Mauch Chunk–Pottsville clastic wedge 1. KY-21-SG Stony Gap (n=310) 200 400 600800 1000 1200 1400 1600 1800 2000 22002400 2600 2800 3000 3200 Detrital Zircon Age (Ma)

Lower Permian Pennington-Lee clastic wedge 21. Greene (Becker et al., 2006; n=78) 20. Washington (Becker et al., 2006; n=83) Upper Pennsylvanian Pennington-Lee clastic wedge 19. Upper Monongahela (Dodson, 2008; n=92)

18. Lower Monongahela (Dodson, 2008; n=172)

17. Conemaugh (Dodson, 2008; n=83) Middle Pennsylvanian Mauch Chunk–Pottsville clastic wedge 16. Sharp Mountain (Gray and Zeitler, 1997; n=44) Middle Pennsylvanian Pennington-Lee clastic wedge

15. Cross Mountain (Thomas et al., 2004a; n=37) Lower Pennsylvanian Mauch Chunk–Pottsville clastic wedge 14. Pottsville (Becker et al., 2005; n=77) t conic Ta & - Figure 4. Relative age-probability plots cadian ville A showing previously published results yolite ntral Plains ans-Hudson y from U-Pb analyses of sandstones in the Superior enokean & an-African– ans-Amazonian Alleghanian Granite Rh Gren Ce P Tr P Brasiliano & Iapetan synrif

Eburnian Tr Appalachian foreland (analytical data, lo- 13. Tumbling Run (Becker et al., 2005; n=26) cation, and stratigraphic information are available in the cited references). Vertical Lower Pennsylvanian Pennington-Lee clastic wedge colored bands represent the age ranges 12. Montevallo (Becker et al., 2005; n=39) of potential provenance provinces in the Appalachians and North American craton. The plots are color coded as in Figures 2 11. Lower Raleigh (Eriksson et al., 2004; n=84) and 3: blue—Mauch Chunk–Pottsville clastic wedge; red—Pennington-Lee clastic wedge; green—longitudinal dispersal sys- Normalized Probabilit 10. Bottom Creek (Grimm et al., 2013; n=155) tem. The plots omit a total of six analyzed grains, which have ages younger than the 9. Pocahontas (Becker et al., 2005; n=61) stratigraphically documented depositional Lower Pennsylvanian longitudinal system ages. 8. Sewanee (Thomas et al., 2004a; n=41)

7. Upper Raleigh (Eriksson et al., 2004; n=67)

6. Lee (Becker et al., 2005; n=58)

5. Raccoon Mountain (Becker et al., 2005; n=68) Upper Mississippian Mauch Chunk–Pottsville clastic wedge 4. Bluestone (Park et al., 2010; n=91)

3. Princeton (Park et al., 2010; n=96)

2. Hinton (Park et al., 2010; n=93)

1. Mauch Chunk (Park et al., 2010; n=96) 200 400 600800 1000 1200 1400 1600 1800 20002200 2400 26002800 3000 3200 Detrital Zircon Age (Ma)

Our Hf isotope data are interpreted within the standard framework of juve Sharon Conglomerate Member of the Pottsville Formation nile (positive) values indicating magma consisting mainly of material extracted (Northern Sample OH-4-SN) from the mantle during or immediately prior to magmatism, versus more evolved (negative) values that record incorporation of significantly older crust. The Sharon Conglomerate Member of the Lower Pennsylvanian Pottsville

Vertical arrays on εHft diagrams are interpreted to represent magmas that Formation in northwestern Pennsylvania and northeastern Ohio laps onto an contain both material derived from the mantle during (or immediately prior erosional unconformity that cuts down section northward to as low as Upper to) magmatism and significantly older crustal materials. For comparison with Devonian strata (Fuller, 1955; Wanless, 1975). Paleocurrents in the Sharon Con- our new data, color-shaded fields in Figure 3 encompass the main clusters of glomerate Member in northwestern Pennsylvania and northeastern Ohio in- data points previously reported for potential provenance provinces (original dicate longitudinal (southwestward) drainage (Fig. 2) (Meckel, 1967) that was data are in the cited references for Figure 3). separated from coeval transverse (northwestward) drainage during Pottsville deposition in eastern Pennsylvania (Edmunds et al., 1999). A sample of the Sharon Conglomerate from northeasternmost Ohio (Fig. 2) has a dominant concentration between 1302 and 972 Ma with a strong peak at 1037 Ma and a RESULTS OF DETRITAL-ZIRCON ANALYSES weak peak at 1162 Ma (Fig. 3). Another prominent concentration at 491–361 Ma has a peak at 443 Ma. Minor concentrations are between 1881 and 1302 Ma New analyses include seven samples for U-Pb age data (Supplemental with peaks at 1648, 1458, and 1366 Ma; and between 682 and 538 Ma with a Table S1 [see footnote 1], Fig. 3) and six samples for Hf isotopic ratios (Sup- peak at 618 Ma. A few grains are scattered between 2846 and 2675 Ma and plemental Table S2 [see footnote 2], Fig. 3). The U-Pb age data are described between 972 and 777 Ma. here in order of depositional age (oldest to youngest) and are placed in the context of the two transverse dispersal systems in the clastic wedges and in the longitudinal system in the distal part of the basin. The Hf isotopic ratios are Sharon Conglomerate Member of the Pottsville Formation described separately. (Southern Sample OH-1-SS)

The sample location in southern Ohio is within the longitudinal dispersal U-Pb Age Data system; however, paleocurrents and paleotopography indicate transverse (northwestward) drainage locally during deposition of the Sharon Conglomer Stony Gap Sandstone Member (Sample KY-21-SG) ate Member (Fuller, 1955; Rice and Schwietering, 1988; Ketering, 1992). The regional drainage and quartz-pebble distribution patterns suggest that the Sandstone was collected from the Upper Mississippian Stony Gap Sand- local variations around the sample site reflect distributaries within the transi- stone Member of the Pennington Formation at a site on the leading edge of tion from the Mauch Chunk–Pottsville transverse drainage into the longitudinal the Appalachian thrust belt in eastern Kentucky in the distal part of the fore- drainage. The sandstone sample has one dominant mode at 1056–894 Ma with land basin (Fig. 2). The sandstone has dominant concentrations of detrital- a peak at 1012 Ma and another at 501–380 Ma with a peak at 465 Ma (Fig. 3). zircon ages in the ranges of 1238–936 Ma and 474–372 Ma with peaks at The sample includes a secondary mode at 1278–1070 Ma with peaks at 1232 1091 and 426 Ma, respectively (Fig. 3). Secondary concentrations are in the and 1182 Ma. The sample also has a minor concentration between 1791 and ranges of 2966–2558 Ma with a peak at 2718 Ma and of 1815–1254 Ma with 1292 Ma with peaks at 1554 and 1332 Ma, and another between 711 and 554 Ma peaks at 1660, 1508, and 1347 Ma. A few grains have ages of 2116–1876 Ma with a peak at 616 Ma. A few ages are scattered at 2695–2418, 2095–1883, and and 637–532 Ma. The Stony Gap Sandstone Member, regionally, is the lower 336–330 Ma. The youngest grain is 330 Ma, which is the age of the earliest member of the Hinton Formation within the Mauch Chunk–Pottsville clas- Alleghanian orogeny and also near the depositional age of the Sharon. Simi- tic wedge northeast of this collecting site (Fig. 2) (e.g., Thomas, in Hatcher larities in the detrital-zircon populations indicate that the two Sharon samples et al., 1989b); the sandstone unit has been correlated to this distal location are parts of the same longitudinal dispersal system. as the Stony Gap Sandstone Member within the Pennington Formation (Group) (e.g., Thomas, 1959; Wilpolt and Marden, 1959). This sample location is within the area of overlap of the Mauch Chunk–Pottsville clastic Corbin Sandstone (Sample KY-18-CB) wedge with the Pennington-Lee clastic wedge, leaving the provenance un- certain; however, regional distribution and inferred continuity of the Stony A sample of the Corbin Sandstone represents the youngest part of the Gap Sandstone Member are consistent with the distal part of the Mauch southwest-directed longitudinal fluvial system along the distal part of Chunk–Pottsville clastic wedge. the Appalachian foreland basin (Fig. 2) (Archer and Greb, 1995; Greb and

Chesnut, 1996). The dominant concentration of detrital-zircon ages is in the weak secondary mode at 1524–1296 Ma has peaks at 1469 and 1339 Ma, and range 1191–924 Ma with a prominent peak at 1076 Ma and a secondary peak another at 488–364 Ma has peaks at 487 and 432 Ma. Minor modes at 1692– at 1176 Ma (Fig. 3). Another important concentration at 1843–1543 Ma has a 1624 and 628–585 Ma have peaks at 1653 and 625 Ma, respectively. A few prominent peak at 1652 Ma and less pronounced peaks at 1808 and 1744 Ma. grains are scattered at 2810–2664, 1855, 1755–1754, 1565–1560, 757–718, and The sample includes strong secondary concentrations at 2813–2531 and 533 Ma. The youngest detrital zircon in this stratigraphically highest sample is 499–406 Ma, with peaks at 2716 and 456 Ma, respectively. Another secondary 364 Ma, within the age range of the Acadian orogeny. concentration at 1543–1211 Ma has peaks at 1502 and 1390 Ma. A few grains are scattered at 3591–2986, 1987–1896, and 822–609 Ma. The concentration of Hf Isotopic Data grains with ages of 2813–2531 Ma, which corresponds to the Superior province of the Canadian Shield, is distinctly greater than in any other samples, except Hafnium isotopic analyses have been conducted on detrital-zircon grains the Mississippian Stony Gap Sandstone Member (sample KY-21-SG) of the from six samples that represent deposition in the two clastic wedges and Pennington Formation, which is stratigraphically below the Corbin Sandstone longitudinal system during Mississippian–Permian time (Fig. 3). For each in the same general area. In contrast, other sandstones (samples OH-4-SN and sample, zircon grains from each age group were analyzed with emphasis on OH-1-SS) of the longitudinal dispersal system have only minor numbers of younger (<800 Ma) grains and on avoiding grains with significant discordance grains of Superior age. or poor precision. Precambrian grains from these samples yield juvenile to intermediate

εHft values, most of which overlap with values from Paleoproterozoic–Meso Grundy-Norton Stratigraphic Interval (Sample VA-1-GN) proterozoic igneous rocks of the Grenville, Granite-Rhyolite, and Central Plains

provinces (Fig. 3). There is no discernible pattern in the εHft values with age or A sample of a sandstone from the Lower Pennsylvanian Grundy-Norton basinal setting. Neoproterozoic grains in both clastic wedges yield εHft values stratigraphic interval in the distal part of the transverse Pennington-Lee dis- that are quite variable, ranging from –13 to +7. persal system (Fig. 2) has a strongly dominant mode of detrital-zircon ages Zircon grains with early Paleozoic U-Pb ages yield interesting geographic at 1252–934 Ma with peaks at 1175 and 1067 Ma (Fig. 3). A secondary mode and temporal patterns (Fig. 3). Using the three phases of Appalachian magma- at 1479–1252 Ma has a peak at 1454 Ma. Minor concentrations at 1770–1544, tism (Taconic, Acadian, and Alleghanian) as a temporal guide, the two clastic 625–517, and 462–322 Ma have peaks at 1588, 619, and 370 Ma, respectively. A wedges and longitudinal system contain abundant Taconic- and Acadian-age few grains are scattered between 2720 and 2659, and at 1895 Ma. The young- grains. Samples from the Pennington-Lee clastic wedge yield mainly interme- est grain at 322 Ma is the only grain with an Alleghanian age; 322 Ma is near diate (–5 to +5) εHft values, which are also present in samples from the Mauch the depositional age of the interval. Chunk–Pottsville clastic wedge and the longitudinal system. Samples from the latter two systems also contain grains with more negative and more positive

εHft values, which suggests that the sources contained more heterogeneous Princess No. 7 Coal (Sample KY-19-PR7) crustal materials than those for the Pennington-Lee clastic wedge.

A sample of a sandstone above the Middle Pennsylvanian (Desmoine- sian) Princess No. 7 coal (Fig. 2) has a dominant peak of detrital-zircon ages at APPALACHIAN POSSIBLE PROVENANCE COMPONENTS 1089 Ma, within a concentration in the range of 1254–901 Ma (Fig. 3). The sample includes a secondary concentration between 1550 and 1254 Ma with peaks Canadian Shield at 1471 and 1318 Ma. Minor concentrations are in the ranges of 1733–1615, 661–551, and 470–373 Ma with peaks at 1656, 631, and 417 Ma, respectively. A The Canadian Shield of the eastern North American craton includes several few grains are scattered at 2763–2668, 2153, and 1839 Ma. distinct age provinces: Superior, Penokean, Central Plains, and Grenville (Fig. 1). These, as well as the Granite-Rhyolite province, are covered by Paleozoic sedimentary rocks across the Midcontinent. Sedimentary thickness and facies dis- Proctor Sandstone Member (Sample WV-1-PR) tributions along the present eroded limits of the Paleozoic cover strata, as well as erosional remnants on the Shield and xenoliths in diatremes, indicate that The Proctor Sandstone Member of the Greene Formation is the youngest much of the Shield was covered before Mississippian time and, therefore, not exposed sandstone in the Dunkard Group in the Permian System in West Vir- available as a primary source of late Paleozoic sediment (Sloss, 1988; Cecile and ginia (Fig. 2). A dominant mode of detrital-zircon ages of 1275–944 Ma has a Norford, 1993). Earlier, during Iapetan rifting of Laurentia and initial passive- prominent peak at 1051 Ma and another peak at 1166 Ma (Fig. 3). A relatively margin transgression (e.g., Sloss, 1988), the exposed craton provided a primary

source of zircons with ages from Superior to Grenville (Fig. 3), which were dis- Gondwanan Accreted Terranes persed irregularly to parts (but not all) of the rifted margin (e.g., Cawood and Nemchin, 2001; Eriksson et al., 2004; Thomas et al., 2004a, 2004b; Allen, 2009; Accreted terranes of Gondwanan affinity extend along the internal parts Chakraborty et al., 2012) and were reworked by passive-margin transgression of the Appalachian orogen (Fig. 1) (e.g., Hatcher et al., 2007; Hibbard et al., (e.g., Konstantinou et al., 2014). The Shield has been interpreted to be a primary 2007; Hatcher, 2010). Three major composite terranes—Ganderia, Avalonia, source of sediment supplied to the distal margins of Appalachian foreland ba- and Meguma—along the orogen from the New York promontory to the New- sins, and these interpretations can be evaluated herein with detrital-zircon data. foundland embayment (Fig. 1) had been accreted by the late Paleozoic (e.g., Hibbard and Karabinos, 2013). From the Pennsylvania embayment southward Grenville Province to the Alabama promontory, the Carolinia composite terrane comprises the internal part of the Appalachian orogen (Fig. 1) (Hibbard, 2000; Hatcher, 2010). The Grenville province encompasses the Elzevirian and Shawinigan orog- The Suwannee terrane (documented by drill data in the subsurface beneath enies and the Ottawan and Rigolet phases of the Grenville orogeny, ranging the Gulf and Atlantic Coastal Plains) was accreted in the Pennsylvanian (Fig. 1) through a time of approximately 1300 to 950 Ma (Fig. 5) (Bartholomew and (Thomas et al., 1989a; Thomas, 2010; Mueller et al., 2014). Hatcher, 2010; Rivers et al., 2012). The Grenville province includes inliers of The Gondwanan terranes have Neoproterozoic metavolcanic, metasedi- older, partially reworked crystalline rocks of various ages, including compo- mentary, and plutonic basement rocks with ages of 800–520 Ma, correspond- nents of the Granite-Rhyolite province (1500–1320 Ma, reworked in the Gren- ing to Pan-African–Brasiliano events in Gondwana (Fig. 5) (e.g., Pollock et al., ville province of southern Canada), the Labrador province (1700–1600 Ma, re- 2010; Willner et al., 2013; Mueller et al., 2014; Henderson et al., 2015); Sm-Nd worked in the Grenville province of eastern Canada) (Rivers et al., 2012), and systematics from the Suwannee terrane indicate interaction with Mesoprotero the Mars Hill terrane (1800 Ma, reworked in the southern part of the Grenvillian zoic (1330–1040 Ma) lithosphere (Fig. 5) (Heatherington et al., 1996; Mueller Blue Ridge external basement massif) (Fig. 1) (Ownby et al., 2004). As shown et al., 2014). Detrital zircons from late Neoproterozoic to Cambrian sedimentary on Figure 3, igneous rocks of the Grenville orogen and sediments derived cover strata generally are dominated by Pan-African–Brasiliano ages of 760–

from these rocks yield εHft values that range from –5 to +10 (Mueller et al., 530 Ma; older components of Gondwana, including ages of 2730–2550 and 2008; Bickford et al., 2010). Relative enrichment in zirconium during the Gren- 2160–1140 Ma, especially Eburnian–Trans-Amazonian ages of 2160–1950 Ma, ville orogeny generated extraordinarily abundant zircons of that age (Moecher are variably represented in the sedimentary detritus (Fig. 6) (Pollock et al., and Samson, 2006), at least partially accounting for the dominant numbers of 2010; Willner et al., 2013; Henderson et al., 2015). Detrital zircons from the Grenville-age zircons in many Paleozoic sandstones. Cambrian to Devonian cover succession of the Suwannee terrane have age Grenville-age rocks exposed in Appalachian external and internal base- concentrations at 650–510 Ma and 2250–2000 Ma (Fig. 6), corresponding to ment massifs (Fig. 1) provide a primary source of detrital zircons with ages Pan-African–Brasiliano and Eburnian–Trans-Amazonian, respectively (Mueller of 1300–950 Ma, as well as some older ages from inliers within the Grenville et al., 1994, 2014). Within the Devonian–Permian fill of the fault-bounded province. Abundant Grenville detrital zircons are available for recycling from composite Maritimes basin (Fig. 1) (e.g., van de Poll et al., 1995), Devonian– post-Grenville Appalachian sandstones. Mississippian sandstones in the St. Marys sub-basin have detrital-zircon age

Alleghanian plutons A Acadian plutons Figure 5. Diagram of ages of potential n=54 primary sources of detrital zircons for the Taconic plutons 350 400450 500 Ma Appalachian foreland. Black bars indicate crystallization ages of zircons; gray bars Iapetan synrift plutonic and volcanic rocks indicate ages of xenocrysts, inclusions, and protoliths within the primary igneous rocks. Data are from references cited in the Gondwanan terranes text. Inset A: Relative age-probability plot of data from Taconic and Acadian igneous Grenville province rocks (from Sinha et al., 2012).

243 5678910 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 Age (×100 Ma)

GEOSPHERE | Volume 13 | Number 6 Thomas et al. | Appalachian detrital zircons Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/13/6/2206/3990899/2206.pdf 2214 by guest on 23 September 2021 Research Paper & conic cadian Ta A Brasiliano Eburnian an-African– Alleghanian P ans-Amazonian Tr GANDERIA, AVALONIA, MEGUMA Devonian–Mississippian basin fill (St. Marys sub-basin), Avalonia, Meguma (Murphy and Hamilton, 2000; n=95)

Cambrian sedimentary cover, Ganderia (Willner et al., 2014; n=302)

y Cambrian sedimentary cover, Ganderia (Fyffe et al., 2009; n=277)

Figure 6. Relative age-probability plots of previously published results from U-Pb analyses of zircons from sedimentary cover rocks in accreted Gondwanan terranes (analytical data, location, and stratigraphic information are available in the cited references). Vertical colored bands Neoproterozoic–Cambrian sedimentary cover, Avalonia (Henderson et al., 2015; n=570) represent the age ranges of potential provenance provinces for sedimentary rocks in Normalized Probabilit Gondwanan accreted terranes. The plots are color coded to distinguish between Neoproterozoic–Cambrian sedimentary cover, Avalonia (Willner et al., 2013; n=432) different Gondwanan terranes.

Early Neoproterozoic, Avalonia (Henderson et al., 2015; n=160)

CAROLINIA Neoproterozoic–earliest Cambrian sedimentary cover, Carolinia (Pollock et al., 2010 n=410)

SUWANNEE Cambrian–Devonian sedimentary cover, Suwannee (Mueller et al., 1994, 2014; n=75 )

ALL (n=2321)

200 400 600800 10001200 1400 1600 1800 2000 2200 2400 2600 2800 3000 3200 Detrital Zircon Age (Ma)

concentrations of 760–550 Ma and 2200–2000 Ma (Fig. 6) (Murphy and Ham- Sandstones in the synrift fill of the Birmingham intracratonic graben (Rome ilton, 2000). As shown on Figure 3, igneous and sedimentary rocks from the Formation, Fig. 7), inboard from the Iapetan rifted margin, have detrital zircons

Gander and Avalon terranes yield εHft values for Meso- and Paleoproterozoic with ages that correspond to each of the provinces of the Laurentian craton grains that are somewhat more evolved than those of North American cratonal from Superior to Grenville (Thomas et al., 2004b). The ages of detrital zircons

provinces, and highly variable εHft values for Neoproterozoic–early Paleozoic available for recycling from the synrift sedimentary rocks vary locally along the grains (Willner et al., 2013, 2014; Henderson et al., 2015; Pollock et al., 2015). rifted margin. Because no rocks older than Grenville, except some inliers in the The accreted terranes are potential sources of detritus for the late Paleozoic Grenville province, are exposed in the Appalachians, recycling from the synrift Appalachian foreland; however, the ages of many of the zircons within the sedimentary rocks is the only available Appalachian source of the older detrital terranes are not distinct from those of other potential Appalachian sources. zircons. Detrital zircons with ages corresponding to those of the synrift igneous Two age ranges are characteristic of Gondwana, 2200–2000 Ma (Eburnian– rocks are rare in the synrift sedimentary rocks. Trans-Amazonian) and 800–520 Ma (Pan-African–Brasiliano); however, Pan- African–Brasiliano zircons cannot be distinguished on the basis of age alone from Iapetan synrift igneous zircons. Although some detrital zircons in the Cambrian–Ordovician Passive-Margin Sedimentary Rocks late Paleozoic Appalachian foreland basin have ages of 2200–2000 and 800– 520 Ma, neither age group is abundant. A classic passive-margin shelf succession of a basal sandstone and over- lying massive carbonate platform records diachronous transition from rift to passive margin and subsequent passive-margin transgression during the Iapetan Synrift Rocks Cambrian (e.g., Sloss, 1988). By the Ordovician, transgression had covered most of the older basement rocks of the Canadian Shield (Sloss, 1988). The Neoproterozoic to Early Cambrian synrift volcanic and plutonic rocks shelf carbonates include widespread interbeds of mature quartzose sandstone (Fig. 1) mark the Iapetan rifted margin of Laurentia (e.g., Thomas, 2014). The and disseminated quartz sand, which were supplied from the Shield and dis- synrift rocks are exposed along Appalachian external basement massifs, re- tributed widely across parts of the carbonate platform by trade winds (e.g., flecting thrust translation of the rifted margin (e.g., Thomas, 1991); however, Pickell, 2012; Konstantinou et al., 2014; Thomas et al., 2016). Outboard from synrift rocks constitute a small proportion of the erosion surface. Synrift rocks the shelf edge, off-shelf mud-dominated slope-and-rise deposits include car- also are distributed along intracratonic synrift fault systems inboard from the bonate mud and quartz sand from the shelf, as well as olistoliths of carbonate Iapetan rifted margin, including igneous rocks along some fault systems and rocks, sandstone, synrift volcanic rocks, and basement rocks (e.g., Viele and sedimentary rocks that fill intracratonic grabens (e.g., Thomas, 2014). Thomas, 1989; Hanson et al., 2016). Synrift igneous rocks along the Iapetan rifted margin range in age from The basal transgressive sandstones of the passive-margin succession are 765 to 530 Ma (Fig. 5) (compilation in Thomas, 2014), but no comprehensive dominated by detrital zircons with ages of 1300–950 Ma (Fig. 8), consistent systematic distribution pattern is evident. Detrital zircons from synrift igne- with sedimentary reworking of the Grenville-age basement rocks during trans- ous rocks (535 ± 5 Ma) along the intracratonic Southern Oklahoma fault sys- gression. Like the synrift sedimentary rocks, the passive-margin succession tem inboard from the Iapetan rifted margin in the Ouachita embayment have locally contains some older zircons. Detrital zircons from the Superior prov-

strongly positive εHft values, indicating juvenile magmas (Thomas et al., 2016); ince dominate the widely distributed quartz sand within the carbonate shelf; however, Hf data are not yet available for synrift igneous rocks along the but zircons from other provinces of the Canadian Shield, including Grenville, Iapetan rift margin in the Appalachians. Synrift igneous rocks are a potential are significant components of the population (Fig. 8) (Pickell, 2012; Konstanti- source of detrital zircons with ages of 765–530 Ma; however, those zircons are nou et al., 2014). In the Ouachita thrust belt, quartz sandstone (Blakely Sand- not distinguishable on the basis of age from Pan-African–Brasiliano zircons in stone, Fig. 8) within the allochthonous off-shelf mud-dominated passive-mar- Gondwanan accreted terranes. gin succession contains detrital zircons that are dominated by ages of the Iapetan synrift fault-bounded basins are almost entirely within the Gren- Grenville and Superior provinces but include ages of other craton provinces ville province (Fig. 1). Some graben-fill synrift accumulations have exclusively (Gleason et al., 2002), suggesting deposition from grain flows that were fed Grenville-age detrital zircons (e.g., Ocoee Supergroup in the Tennessee em- by trade-wind–driven sand dispersal across the carbonate platform and over bayment, Fig. 7) (Bream et al., 2004; Chakraborty et al., 2012), indicating local the shelf edge onto the continental slope. Although no grain-flow deposits sediment dispersal from basement block uplifts. In contrast, other synrift ac- have been recognized along the Appalachian thrust belt, and no quartz sands cumulations along the Iapetan margin have a mixture of detrital-zircon ages within the carbonate platform are known to extend to the Appalachian shelf from Grenville to Superior, indicating widespread dispersal of sediment from edge, the example from the Ouachita thrust belt suggests another possible the Laurentian craton to the rift basins along the margin (e.g., Irishtown and component for recycling in addition to the other passive-margin components Summerside Formations, Fig. 7) (Cawood and Nemchin, 2001; Allen, 2009). in the Appalachians.

NEWFOUNDLAND EMBAYMENT AND ST. LAWRENCE PROMONTORY Irishtown (Allen, 2009; n=69)

Summerside CB-259 (Allen, 2009; n=62) y

Summerside CB-219 (Allen, 2009; n=63)

South Brook CB-212 (Allen, 2009; n=57) Normalized Probabilit

South Brook CB-230 (Allen, 2009; n=54)

TENNESSEE EMBAYMENT Unicoi (Eriksson et al., 2004; n=100)

Ocoee (Chakraborty et al., 2012; n=1077) INTRACRATONIC SYNRIFT BIRMINGHAM GRABEN Rome (Thomas et al., 2004b; n=106)

ALL (n=1588) 200 400 600800 1000 1200 1400 1600 1800 200022002400 260028003000 3200 Detrital Zircon Age (Ma)

Figure 7. Relative age-probability plots of previously published results from U-Pb analyses of zircons from synrift sedimentary rocks along the Iapetan rifted margin of Laurentia (analytical data, location, and stratigraphic information are available in the cited references). Vertical colored bands represent the age ranges of potential provenance provinces in the North American craton, as well as Iapetan synrift igneous rocks. The plots are color coded to distinguish between different parts of the rifted margin and a synrift intracratonic graben.

Cambrian and Ordovician carbonate shelf (Pickell, 2012; Konstantinou et al., 2014; n=2407)

OUACHITA EMBAYMENT AND OFF SHELF Blakely (Gleason et al., 2002; n=21) y

NEWFOUNDLAND EMBAYMENT AND ST. LAWRENCE PROMONTORY Bradore (Allen, 2009; n=60)

QUEBEC EMBAYMENT AND NEW YORK PROMONTORY Potsdam, Poughquag, Hardyston, Cheshire, and Normalized Probabilit Dalton (Satkoski, 2013; n=553)

PENNSYLVANIA EMBAYMENT AND VIRGINIA PROMONTORY Antietam, Weverton, Loudon, and Unicoi (Satkoski, 2013; n=1385)

Erwin and Hardyston (Eriksson et al., 2004; n=160) TENNESSEE EMBAYMENT AND ALABAMA PROMONTORY Hesse, Nebo, Cochran, Unicoi, and Chilhowee (Satkoski, 2013; n=772)

ALL (n=5358)

200 400 600800 1000 12001400 1600 1800200022002400 2600 280030003200 Detrital Zircon Age (Ma)

Figure 8. Relative age-probability plots of previously published results from U-Pb analyses of zircons from passive-margin sedimentary rocks along the Laurentian shelf and shelf margin (analytical data, location, and stratigraphic information are available in the cited references). Vertical colored bands represent the age ranges of potential provenance provinces in the North American craton, as well as Iapetan synrift igneous rocks. The plots are color coded to distinguish between different parts of the passive margin and adjacent craton.

Taconic Synorogenic Rocks confirm syndepositional volcanism during Devonian orogenic events (Tucker et al., 1998). As shown on Figure 3, detrital grains in sediments derived from The Taconic orogeny included a succession of arc-accretion events and the southern Appalachians include Acadian-age zircons with highly variable

foreland subsidence (Drake et al., 1989). Zircons with ages between 490 and (–10 to +6) εHft values (Mueller et al., 2008). 420 Ma generally correspond in age to the Taconic orogeny (Fig. 5), defined in Sandstones in the Acadian clastic wedge are potential sources for late Paleo the broadest sense (e.g., Drake et al., 1989). The eroded roots of Taconic vol- zoic recycling. In addition to data from seven previously published analyses from canic systems have ages of 490–440 Ma (Shaw and Wasserburg, 1984; Tucker the Acadian clastic wedge centered on the Pennsylvania embayment, Figure 10 and Robinson, 1990; Sevigny and Hanson, 1993; Sinha et al., 1997; Karabinos shows data from one newly analyzed sample from the Devonian Frog Moun- et al., 1998; Coler et al., 2000; Miller et al., 2000; Aleinikoff et al., 2002). Succes- tain Sandstone (sample AL-2-FM; Supplemental Table S3 [see footnote 3]) on sively accreted magmatic arcs along the southern part of the New York prom- the Alabama promontory. The marine reworked Frog Mountain Sandstone has ontory have ages of 485–470 Ma (east-dipping subduction) and 454–442 Ma multiple internal unconformities and ranges in age from Early through Middle (west-dipping subduction) (Karabinos et al., 1998). Along the Virginia prom- Devonian or younger (Ferrill, 1984); the feldspathic sandstones indicate base- ontory and Pennsylvania embayment, zircons from a pre-collisional arc com- ment sources along the orogen (Ferrill and Thomas, 1988). The Acadian synoro- plex have ages of 489–470 Ma and from synorogenic arc plutons have ages of genic sandstones have abundant Grenville-age zircons; however, Taconic-age 472–441 Ma; plutons associated with post-orogenic delamination have ages grains dominate some samples (Fig. 10). The Acadian sandstones include the of 438–423 Ma (Sinha et al., 2012). Other examples along the margin have a same variety of older ages as in the Taconic clastic wedge (Fig. 10). Acadian similar history (van Staal et al., 2007; Tull et al., 2014). Widespread K-bentonite synorogenic zircons generally are rare in the Acadian clastic wedge (Fig. 10). beds in the foreland stratigraphy include zircons with U-Pb ages of 453.1 ± 1.3 Table S3. Zircon U-Pb geochronologic analyses by laser ablation–multicollector–inductively coupled plasma mass spectrometry: Ordovician and Devonian sandstones and 454.5 ± 0.5 Ma (Tucker and McKerrow, 1995). As shown on Figure 3, detrital Isotope ratios Apparent ages (Ma) Alleghanian Synorogenic Rocks Analysis U206Pb U/Th 206Pb*±207Pb* ± 206Pb* ±error 206Pb* ±207Pb*±206Pb* ± Best age ±Conc (ppm)204Pb 207Pb* (% 2s )235U*(% 2s ) 238U (% 2s )corr. 238U*(Ma 2s )235U(Ma 2s )207Pb* (Ma 2s )(Ma)(Ma 2s )(%) grains in sediments derived from the southern Appalachians include Taconic- Sample AL-1-CM—Colvin Mountain Sandstone—33° 50' 37.0'' N, 86° 03' 02.3'' W AL-1-CM-98 58 24719 1.016.8264 9.00.7778 9.10.0949 1.90.20584.6 10.4 584.340.6 582.9 194.7584.6 10.4 100.3 AL-1-CM (E2-1)-2 862 60055 4.916.1804 0.30.8789 0.90.1031 0.90.94632.8 5.2640.4 4.3 667.3 6.6632.8 5.294.8 AL-1-CM-85 288 209204 1.416.0222 1.30.9446 1.80.1098 1.20.68671.4 7.8675.3 8.8 688.3 27.8 671.47.8 97.5 AL-1-CM (E2-1)-3 99 78811 1.317.5088 0.30.8828 0.70.1121 0.70.93684.9 4.3642.5 3.4 496.0 5.9684.9 4.3 138.1 age zircons with highly variable (–12 to +6) εHf values (Mueller et al., 2008). Alleghanian plutons (Fig. 5) in the southern Appalachian Piedmont have AL-1-CM (E2-1)-2 796 93948 5.116.7701 0.30.9445 0.80.1149 0.80.93701.0 5.3675.2 4.2 590.2 6.6701.0 5.3 118.8 t AL-1-CM (E2-1)-1 1445 118043 1.715.7754 1.31.0698 2.20.1224 1.80.81744.4 12.6 738.711.6 721.3 27.4 744.4 12.6 103.2 AL-1-CM (E2-1)-3 25 35168 0.414.5338 6.81.6266 7.40.1715 2.90.391020.127.4980.5 46.4 892.9 140.3892.9 140.3 114.2 AL-1-CM (E2-1)-2 49 49188 1.814.3081 3.91.6405 8.10.1702 7.10.881013.466.8985.9 51.3 925.2 80.1 925.2 80.1 109.5 AL-1-CM-40 80 24115 2.014.2860 3.51.5076 3.90.1562 1.80.46935.7 15.9 933.524.1 928.3 71.8 928.3 71.8 100.8 Taconic synorogenic clastic wedges are potential sources for late Paleo- ages of 330–300 Ma (Sinha and Zietz, 1982; Samson et al., 1995; Coler et al., AL-1-CM (E2-1)-2 63 24897 0.814.2436 2.91.5331 3.50.1584 1.90.54947.8 16.5 943.721.2 934.4 59.5 934.4 59.5 101.4 AL-1-CM (E2-1)-2 110 26548 2.313.8943 1.81.7022 3.20.1715 2.60.811020.624.21009.420.2 985.1 37.3 985.1 37.3 103.6 AL-1-CM (E2-1)-1 101 54726 1.613.8897 3.61.7031 4.60.1716 2.80.611020.826.41009.729.3 985.8 73.6 985.8 73.6 103.5 AL-1-CM-31 59 21035 1.113.8758 4.31.6402 4.60.1651 1.70.36984.9 15.3 985.829.1 987.8 87.6 987.8 87.699.7 AL-1-CM (E2-1)-2 210 42005 3.913.8645 1.91.7409 2.70.1751 1.90.721039.918.61023.817.4 989.5 38.1 989.5 38.1 105.1 zoic recycling. Figure 9 illustrates data from ten previously published analyses 2000), whereas those in New England have ages of 330–270 Ma (Aleinikoff AL-1-CM (E2-1)-3 23 50775 0.713.8477 3.21.6452 10.10.1652 9.60.95985.8 87.8 987.764.0 992.0 65.1 992.0 65.199.4 AL-1-CM-32 108 70716 2.013.8444 1.81.5833 2.10.1590 1.10.53951.1 9.9963.7 13.3 992.5 36.8 992.5 36.895.8 AL-1-CM-15 79 36905 2.013.8421 2.01.7423 2.60.1749 1.80.671039.117.01024.317.1 992.8 40.0 992.8 40.0 104.7 AL-1-CM-42 61 52361 1.113.8413 2.01.6194 2.30.1626 1.00.45971.0 9.2977.7 14.3 992.9 41.4 992.9 41.497.8 AL-1-CM-26 524 11806 1.813.8141 0.51.4533 5.70.1456 5.61.00876.3 46.3 911.234.1 996.9 11.0 996.9 11.0 87.9 from Taconic clastic wedges, as well as from one newly analyzed sample from et al., 1985; Zartman and Hermes, 1987; Tomascak et al., 1996). Tonsteins (vol- AL-1-CM-44 176 60866 2.813.7919 1.41.6386 1.50.1639 0.70.45978.4 6.3985.2 9.7 1000.228.01000.2 28.097.8 AL-1-CM (E2-1)-2 229 46049 5.413.7904 2.31.7331 6.40.1733 5.90.931030.556.61020.941.2 1000.447.71000.4 47.7 103.0 AL-1-CM-30 111 72069 1.813.7802 1.71.7622 2.40.1761 1.70.711045.716.61031.615.8 1001.934.91001.9 34.9 104.4 AL-1-CM (E2-1)-2 367 203984 5.113.7708 1.81.7082 2.50.1706 1.70.691015.416.11011.615.9 1003.336.61003.3 36.6 101.2 AL-1-CM-83 142 42985 2.213.7684 1.51.7073 1.70.1705 0.90.511014.88.2 1011.311.0 1003.630.11003.6 30.1 101.1 the lower Upper Ordovician Colvin Mountain Sandstone (sample AL-1-CM; canic ash beds) within Pennsylvanian-age coal beds in the Appalachian basin AL-1-CM-43 91 130476 2.013.7677 1.81.6888 1.90.1686 0.60.331004.66.0 1004.312.4 1003.737.11003.7 37.1 100.1 AL-1-CM-89 60 77784 0.713.7468 4.21.7090 4.40.1704 1.30.291014.211.91011.927.9 1006.884.61006.8 84.6 100.7 AL-1-CM-74 109 65825 2.213.7321 1.41.7152 1.80.1708 1.10.611016.710.21014.211.3 1009.028.31009.0 28.3 100.8 AL-1-CM (E2-1)-3 13 29424 0.613.7229 4.31.7486 8.00.1740 6.80.841034.364.51026.651.7 1010.387.01010.3 87.0 102.4 3 AL-1-CM-82 43 21685 1.113.7212 4.11.7631 4.30.1755 1.30.311042.112.81032.028.0 1010.683.31010.6 83.3 103.1 Supplemental Table S3 ) on the Alabama promontory in the marine reworked have ages of 316 ± 1 Ma (Upper Banner coal; U-Pb zircon) and 311.2 ± 0.7 Ma AL-1-CM-05 96 92598 2.113.7097 1.11.7662 1.90.1756 1.50.791043.014.21033.112.0 1012.323.01012.3 23.0 103.0 AL-1-CM (E2-1)-2 83 502931 3.213.7080 4.31.6956 5.00.1686 2.60.511004.323.91006.932.1 1012.587.51012.5 87.599.2 AL-1-CM-49 47 16164 1.113.6980 4.71.7208 4.80.1710 1.00.201017.49.2 1016.331.0 1014.095.71014.0 95.7 100.3 AL-1-CM-37 70 45611 2.213.6952 3.31.7764 4.20.1764 2.70.631047.525.81036.927.6 1014.467.01014.4 67.0 103.3 40 39 AL-1-CM (E2-1)-1 82 31245 1.513.6809 2.21.7624 3.00.1749 2.10.691038.920.11031.719.7 1016.644.61016.6 44.6 102.2 distal southwestern part of a clastic wedge centered on the Tennessee embay- (Fire Clay coal; Ar/ Ar), respectively (Lyons et al., 1992, 1997; Kunk and Rice, AL-1-CM (E2-1)-2 226 75479 2.513.6797 1.91.7398 5.30.1726 5.00.941026.547.41023.434.4 1016.737.61016.7 37.6 101.0 AL-1-CM-47 91 86594 2.113.6773 1.91.7466 2.40.1733 1.40.581030.113.21025.915.4 1017.139.31017.1 39.3 101.3 AL-1-CM (E2-1)-2 116 37153 3.513.6728 2.11.7552 2.70.1741 1.80.651034.416.71029.117.5 1017.841.61017.8 41.6 101.6 AL-1-CM (E2-1)-2 210 83828 4.213.6725 1.61.7722 3.60.1757 3.20.891043.631.31035.323.7 1017.833.41017.8 33.4 102.5 AL-1-CM-110175 99061 2.613.6722 1.51.7357 2.20.1721 1.60.741023.815.41021.914.2 1017.830.31017.8 30.3 100.6 ment (Bayona and Thomas, 2006). Grenville ages dominate the detrital-zircon 1994). As shown in the reference field in Figure 3, detrital grains in sediments AL-1-CM (E2-1)-2 298 42440 3.313.6716 1.21.6816 2.10.1667 1.80.83994.1 16.2 1001.613.4 1017.923.51017.9 23.597.7 populations in the Taconic clastic wedges (Fig. 9). Lesser components of the derived from the southern Appalachians include Alleghanian-age zircons with 3 Supplemental Table S3. Zircon U-Pb geochronologic Taconic detrital-zircon population represent pre-Grenville Laurentian cratonic highly variable (–8 to +6) εHf values (Mueller et al., 2008). analyses by laser ablation–multicollector–inductively t coupled plasma mass spectrometry: Ordovician provinces, most abundantly Granite-Rhyolite from recycling or from Gren- Zircons with ages of the Grenville province and the Taconic and Acadian and Devonian sandstones. Please visit http://doi ville inliers, and also minor concentrations of Central Plains, Penokean, and synorogenic plutons dominate the detrital-zircon populations of the Allegha- .org/10 .1130/GES01525 .S3 or the full-text article on Superior ages (Fig. 9). Although synorogenic igneous rocks potentially are nian clastic wedges, which contain less abundant zircons from other recycled www.gsapubs.org to view the Supplemental Table. available as primary sources of detrital zircons, only one sandstone analyzed pre-Alleghanian primary sources (Figs. 3, 4). Although Alleghanian synoro- from the Taconic synorogenic clastic wedges has zircon grains (two) of Taconic genic igneous rocks are scattered along the orogen (e.g., Hibbard and Kara age (Fig. 9) (Park et al., 2010), indicating no significant source for recycling of binos, 2013), only seven detrital zircons in the 3564 reported analyses (both Taconic-age zircons from Taconic synorogenic sandstones. new and previously published) have ages younger than 331 Ma (Figs. 3, 4).

Acadian Synorogenic Rocks PROVENANCE OF MISSISSIPPIAN–PERMIAN SANDSTONES IN THE APPALACHIAN FORELAND Separate phases of the Acadian orogeny reflect accretion of composite terranes along the Laurentian margin (e.g., Hibbard and Karabinos, 2013). Mauch Chunk–Pottsville Clastic Wedge Plutons contemporaneous with the Acadian orogeny (420–350 Ma; Fig. 5) are more common in the northern Appalachians than in the southern Appala- One new analysis and seven previously published analyses characterize the chians (Osberg et al., 1989; Eusden et al., 2000; Miller et al., 2000; Hibbard and Mauch Chunk–Pottsville clastic wedge (Fig. 2). The stratigraphically lowest and Karabinos, 2013). Acadian plutons in the Pennsylvania embayment have ages most distal sample is from the Upper Mississippian Stony Gap Sandstone Mem- of 381–362 Ma (Sinha et al., 2012). Bentonite beds in the Appalachian foreland ber (sample KY-21-SG, Figs. 2, 3). Published data include Upper Mississippian

GEOSPHERE | Volume 13 | Number 6 Thomas et al. | Appalachian detrital zircons Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/13/6/2206/3990899/2206.pdf 2219 by guest on 23 September 2021 Research Paper t e & e- ville yolit conic Rh Granit Ta Gren Superior ntral Plains Eburnian enokean & an-African– Brasiliano & P ans-Hudson P Ce Tr Iapetan synrif ans-Amazonian Tr NEWFOUNDLAND EMBAYMENT AND ST. LAWRENCE PROMONTORY American Tickle (Cawood and Nemchin, 2001; n=58)

QUEBEC EMBAYMENT AND NEW YORK PROMONTORY Austin Glen/Normanskill (McLennan et al., 2001; n=41)

PENNSYLVANIA EMBAYMENT AND VIRGINIA PROMONTORY Shawangunk (Gray and Zeitler, 1997; McLennan et al., 2001; n=49)

Figure 9. Relative age-probability plots of results from U-Pb analyses of zircons Rose Hill (Park et al., 2010; n=99) from sedimentary rocks in Taconic synorogenic clastic wedges in the Appalachians y (analytical data and location information for sample AL-1-CM are in Supplemental Keefer (Park et al., 2010; n=97) Table S3 [see footnote 3]; analytical data, location, and stratigraphic information for previously published analyses are available in the cited references). Vertical Tuscarora (Park et al., 2010; n=93) colored bands represent the age ranges of potential provenance provinces in the North American craton, Iapetan synrift ig- Bald Eagle/Oswego (Park et al., 2010; n=98) neous rocks, Taconic synorogenic igneous

Normalized Probabilit rocks, and Gondwanan accreted terranes. The plots are color coded to distinguish between different Taconic clastic wedges along the Appalachians.

Eagle Rock (Eriksson et al., 2004; n=48)

Bays (Eriksson et al., 2004; n=89)

Fincastle/Martinsburg (Park et al., 2010; n=98)

TENNESSEE EMBAYMENT AND ALABAMA PROMONTORY Colvin Mountain (AL-1-CM) (n=229)

ALL (n=999)

200 400 600800 100012001400 160018002000220024002600280030003200 Detrital Zircon Age (Ma)

GEOSPHERE | Volume 13 | Number 6 Thomas et al. | Appalachian detrital zircons Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/13/6/2206/3990899/2206.pdf 2220 by guest on 23 September 2021 Research Paper t & e- ville conic yolite cadian Ta A Superior Rh Granit Gren enokean & ntral Plains Eburnian P ans-Hudson an-African– Brasiliano & P Ce Tr Iapetan synrif ans-Amazonian Tr

PENNSYLVANIA EMBAYMENT AND VIRGINIA PROMONTORY Price (Park et al., 2010; n=95)

Figure 10. Relative age-probability plots of

y Walton/Catskill (McLennan et al., 2001; n=45) results from U-Pb analyses of zircons from sedimentary rocks in the Acadian synorogenic clastic wedge in the Appalachians (analytical data and location information for sample AL-2-FM are in Supplemental Hampshire (Park et al., 2010; n=95) Table S3 [see footnote 3]; analytical data, location, and stratigraphic information for previously published analyses are available in the cited references). Vertical colored bands represent the age ranges of potential provenance provinces in the North American craton, Iapetan synrift ig- Normalized Probabilit Cloyd/Chemung (Eriksson et al., 2004; n=86) neous rocks, Taconic and Acadian synorogenic igneous rocks, and Gondwanan accreted terranes. The plots are color coded to distinguish between the Acadian clastic wedge and distal foreland along the Appa Chemung/Greenland Gap (Park et al., 2010; n=98) lachians.

Foreknobs (Park et al., 2010; n=99)

Ridgeley/Oriskany (Park et al., 2010; n=96)

ACADIAN DISTAL FORELAND Frog Mountain (AL-2-FM) (n=284)

ALL (n=898) 200 400 600800 1000 120014001600 1800200022002400 2600 280030003200 Detrital Zircon Age (Ma)

sandstones in the proximal (Mauch Chunk Formation) and southwestern The Lower Pennsylvanian Sharon Conglomerate in the northern part of the mid-distal parts (Hinton Formation, Princeton Sandstone, and Bluestone For- longitudinal system (Fig. 2) laps onto an unconformity, and the sandstones mation) of the clastic wedge (Figs. 2, 4) (Park et al., 2010). Lower Pennsylvanian assigned to the Sharon may not be laterally continuous (e.g., Ruppert et al., (Tumbling Run Member of the Pottsville Formation and Pottsville Formation 2010). Nevertheless, the detrital-zircon populations are similar (Fig. 3). Both undifferentiated; Becker et al., 2005) and Middle Pennsylvanian (Sharp Moun- Sharon samples (OH-4-SN and OH-1-SS, Fig. 3) have prominent Grenville tain Member of the Pottsville Formation; Gray and Zeitler, 1997) sandstones modes and a more dominant Taconic–Acadian peak. In both samples, a minor are from the proximal part of the Mauch Chunk–Pottsville clastic wedge (Figs. peak at 618–616 Ma is the strongest representation in any of the Mississippian– 2, 4). Within the regional context of generally cratonward paleocurrents, south- Permian Appalachian sandstones of ages equivalent to either Iapetan synrift ward paleocurrents in the Sharp Mountain Member of the Pottsville Formation rocks or accreted Gondwanan Pan-African–Brasiliano terranes (Fig. 3); in con-

indicate longitudinal sediment dispersal (Meckel, 1967; Robinson and Prave, trast to positive εHft values from synrift rocks in Oklahoma (Thomas et al.,

1995); however, this system directly overlies an unconformity. 2016), the generally negative εHft values in Sharon sample OH-1-SS (Fig. 3) A consistent concentration of ages in all eight samples indicates a Gren- favor accreted terranes. The Sharon samples contain a few older grains, in- ville source (Figs. 3, 4, 11), either primary from Appalachian massifs or recy- cluding Superior. cled. Another prominent concentration indicates Taconic and Acadian sources Farther south, downstream (Fig. 2), the Corbin Sandstone (sample KY-18-CB, within the Appalachian orogen. The Taconic–Acadian peak exceeds or equals Fig. 3) has both Grenville and Taconic–Acadian concentrations; the Grenville is the Grenville peak, except that the Taconic–Acadian peak decreases upward more dominant. In the Corbin Sandstone, distinct secondary concentrations through the two stratigraphically higher samples in the Upper Mississippian have ages of the Superior (2813–2531 Ma) and Central Plains (1845–1540 Ma) part (Princeton and Bluestone, Fig. 4) of the clastic wedge. The Taconic–Aca- provinces; but these ages are very weakly expressed in both Sharon samples dian peak is even more dominant in the Lower Pennsylvanian sandstones than (Fig. 3). The substantial downstream increase of these components suggests in the underlying Mississippian sandstones (Figs. 4, 11). A secondary concen- introduction of locally derived sediment from one of the transverse systems. tration in all eight samples corresponds to the Granite-Rhyolite province, from The general paucity of grains older than Granite-Rhyolite in the other Missis- either inliers in Grenville terranes or recycling from synrift clastic deposits sippian–Permian sandstones distinguishes the Upper Mississippian Stony Gap (Figs. 3, 4, 11). All of the samples have a few grains with ages that correspond Sandstone Member (sample KY-21-SG, Fig. 3) and the Corbin Sandstone as to ages of Iapetan synrift igneous rocks or accreted Gondwanan Pan-African– the only ones with substantial Superior and Central Plains detritus, suggesting Brasiliano terranes (Figs. 3, 4). The Stony Gap Sandstone Member has dis- some unique local provenance for the Stony Gap and either recycling or con- tinct secondary concentrations of Superior and Central Plains ages (sample tinuing supply for the Corbin. KY-21-SG, Fig. 3), in contrast to most samples from the Mauch Chunk–Pottsville Published data from four sandstones (Raccoon Mountain Formation; Lee clastic wedge (Fig. 4); the Hinton sample (Fig. 4) (Park et al., 2010) from the Formation; upper Raleigh Sandstone, equated to Sewanee Sandstone by Grimm more proximal part of the clastic wedge has a similar but smaller concentra- et al., 2013; and Sewanee Conglomerate; Fig. 4) represent the longitudinal flu- tion of Superior and Central Plains zircons, suggesting a common provenance vial system south of the Corbin sample site (Fig. 2). In each of these sandstones and dispersal pathway. Because of the distance and isolation from primary except the Sewanee, the dominant concentration is of Grenville age (Fig. 4). A sources in the Canadian Shield, the Superior and Central Plains zircons sug- secondary concentration of Taconic–Acadian age varies from sample to sample, gest probable recycling from synrift sedimentary rocks of the Iapetan rifted from dominant in the Sewanee to lacking in the Lee (Fig. 4). The four samples margin or from passive-margin strata (e.g., Thomas et al., 2004a, 2004b). The each have secondary concentrations of Central Plains and Superior ages, but similarities in detrital-zircon populations support assignment of the Stony Gap these are weaker than the equivalent concentrations in the Corbin (Figs. 3, 4). to the dispersal system of the Mauch Chunk–Pottsville clastic wedge rather Because of a lack of an obvious source in the Appalachians, the minor con- than the Pennington-Lee clastic wedge. centration of Superior grains in the upper Raleigh has been inferred to indicate a primary source in the Canadian Shield for the longitudinal sandstones Longitudinal Fluvial System (Eriksson et al., 2004; Grimm et al., 2013). The scarcity of Superior-age grains in the Sharon samples in the northern, more upstream sandstones some- The Early Pennsylvanian longitudinal fluvial system of quartzarenites and what isolates the concentration of Superior-age grains in the Corbin (Fig. 3) quartz-pebble conglomerates trends southwestward along the distal side of and sandstones farther south (Fig. 4). Along with a secondary concentration the Appalachian foreland basin (Archer and Greb, 1995). On the basis of paleo of Superior-age grains in the proximal Lower Pennsylvanian Tumbling Run currents and distribution of quartz pebbles, previous interpretations have (Fig. 4), the strong secondary concentration in the distal Upper Mississippian focused on southwestward dispersal of sediment from a source on the north, Stony Gap (Fig. 3) indicates probable dispersal through a somewhat restricted either the Canadian Shield or the northern Appalachians (e.g., Siever and southern part of the transverse Mauch Chunk–Pottsville clastic wedge to feed Potter, 1956; Meckel, 1967). the longitudinal system with recycled grains from Iapetan synrift deposits or

Pennington-Lee clastic wedge Mauch Chunk–Pottsville clastic wedge - t t & e & e e- ville ville conic yolit conic yolit cadian cadian Ta Ta A A Superior Rh Granit Superior Rh Granite Gren Gren Eburnian enokean & enokean & Eburnian ntral Plains ntral Plains Alleghanian Alleghanian P P ans-Hudson ans-Hudson Ce Ce Tr Tr ans-Amazonian ans-Amazonian Tr Tr an-African–Brasiliano an-African–Brasiliano P & Iapetan synrif P & Iapetan synrif r Lowe

Permian (N=3; n=395) r Penn . Uppe (N=4; n=347)

(N=2; n=321) (N=1; n=44) Penn. Middle y t o r n & e- vill e conic adia n yolite Ta Ac Rh Granit Superio Gren nokean & ntral Plains Eburnian Alleghanian Pe ans-Hudson longitudinal system Ce Tr ans-Amazonia Tr Penn . Lower n-African–Brasilian

Pa & Iapetan synrif (N=7; n=1055)

200600 10001400 1800 2200 2600 3000 Normalized Probabilit

(N=2; n=103) Penn . Lower (N=5; n=613) r (N=5; n=686) Miss. Uppe

200600 1000 1400 1800 2200 2600 3000 200600 1000 1400 1800 2200 2600 3000 Detrital Zircon Age (Ma)

Figure 11. Composite relative age-probability plots (derived from data in Figs. 3 and 4) to illustrate variations through the stratigraphic succession and between the Mauch Chunk–Pottsville clastic wedge, Pennington-Lee clastic wedge, and Early Pennsylvanian longitudinal dispersal system in the Appalachian foreland. Vertical colored bands represent the age ranges of potential provenance provinces in the Appa- lachians and North American craton. The plots are color coded as in Figures 2, 3, and 4: blue—Mauch Chunk–Pottsville clastic wedge; red—Pennington-Lee clastic wedge; green—longitudinal dispersal system. Penn.—Pennsylvanian; Miss.—Mississippian; N—number of separate samples; n—number of individual grain analyses.

passive-margin sandstones (e.g., Thomas et al., 2004a). The secondary Central tic wedge. Three samples from lower Permian sandstones (WV-1-PR, Fig. 3; Plains concentrations in the Corbin and longitudinal sandstones to the south Washington Formation and Greene Formation, Fig. 4) (Becker et al., 2006) rep- also contrast with minor components in the Sharon samples but are similar to resent the upper part of the clastic wedge. a secondary concentration in the Stony Gap (Figs. 3, 4). The strong Taconic– All of the samples have a dominant Grenville concentration (Figs. 3, 4, 11); Acadian peaks in the Sharon samples require a source in the Appalachians other components of the detrital-zircon population vary with stratigraphic level. rather than in the Canadian Shield for the upstream components of the longi- Except for a small Acadian peak in the Bottom Creek, the Lower Pennsylvanian tudinal system. sandstones have few to no grains with Taconic or Acadian ages (Figs. 3, 4, 11). Differences in details of peak ages suggest variations in sediment input The contrast in relative abundance of Taconic–Acadian grains suggests an im- along the longitudinal fluvial system. In the downstream direction along the portant difference in proportion of components in the respective provenance longitudinal system, the Taconic–Acadian peak is more prominent than regions of the Pennington-Lee and Mauch Chunk–Pottsville clastic wedges (Fig. the Grenville peak in the two Sharon samples, somewhat reduced in the Corbin 11), a distinction also indicated by Hf ratios (Fig. 3). Above the Lower Pennsyl- sample, lacking in the Lee sample, greater than Grenville in the Sewanee sam- vanian, however, most sandstones in the Pennington-Lee clastic wedge have ple, and reduced in the upper Raleigh and Raccoon Mountain samples (Fig. 4). Taconic–Acadian peaks equal to or greater than the Grenville peaks, similar The stronger Taconic–Acadian peak is similar to that in most samples from to the Mauch Chunk–Pottsville clastic wedge (Fig. 11). The evident upward in- the Mauch Chunk–Pottsville clastic wedge, suggesting that the transverse sys- crease in Taconic–Acadian grains may reflect greater unroofing and/or more tem fed the longitudinal system in the north. The southward decrease in the extensive integration of drainage networks, perhaps paralleling progressive Taconic–Acadian peak is consistent with a lesser Taconic–Acadian component increase in depth of unroofing as indicated by petrographic data (Davis and in the Lower Pennsylvanian part of the Pennington-Lee clastic wedge; how- Ehrlich, 1974). Although the stratigraphically lower Cross Mountain has a domi ever, the non-systematic variation suggests local inputs at various times. nant Taconic–Acadian concentration (Fig. 4), the younger sandstone above the Princess No. 7 coal has only a minor Taconic–Acadian concentration (Fig. 3), Pennington-Lee Clastic Wedge indicating an irregular upward increase through the Middle Pennsylvanian. Generally, the sandstones in the Pennington-Lee clastic wedge have mod- Detrital-zircon age data for the Pennington-Lee clastic wedge are from sam- erate concentrations of Granite-Rhyolite age (Figs. 3, 4, 11), but older ages ples scattered through the stratigraphic succession from Lower Pennsylvanian of detrital zircons are rare. An exception is the Middle Pennsylvanian Cross to lower Permian (Fig. 2). Data from one new sample (VA-1-GN, Fig. 3) and Mountain sample, which has minor concentrations of Central Plains and three published samples (Pocahontas Formation; Bottom Creek Formation; and Superior ages (Fig. 4). lower Raleigh Sandstone, equated to Bottom Creek Formation by Grimm et al., Although depositional ages of the Pennington-Lee clastic wedge overlap 2013; Fig. 4) (Eriksson et al., 2004; Becker et al., 2005; Grimm et al., 2013) rep- the ages of Alleghanian synorogenic igneous rocks, only six grains with Alle resent the Lower Pennsylvanian deposits of the transverse dispersal system ghanian ages have been documented in the clastic wedge. In Lower Pennsyl- in the proximal part of the north-northwestward–prograding Pennington-Lee vanian sandstones, detrital zircons with ages of 325 Ma in the Bottom Creek clastic wedge (Fig. 2). In addition, a sample of Lower Pennsylvanian coarse (Fig. 4) and 322 Ma in the Grundy-Norton (sample VA-1-GN, Fig. 3) are the polymictic conglomerate associated with the Montevallo coal zone in the upper only grains with ages as young as the Alleghanian orogeny; both ages are part of the Pottsville Formation (stratigraphically higher than the reported sam- approximately equal to the stratigraphically documented depositional ages of ples from farther north) in the Appalachian thrust belt in Alabama is from the the sampled horizon. The Monongahela samples include zircon grains with most distal southwestern fringe of the Pennington-Lee clastic wedge (Fig. 2). ages of 322 and 315 Ma (Fig. 4). Two lower Permian sandstones have one In contrast to the regional Pennington-Lee dispersal system, however, in the detrital-zircon grain each (305 Ma in Greene, 314 Ma in Washington; Fig. 4) Montevallo coal zone, the coarse lithic clasts are within a braid plain with within the age range of the Alleghanian orogeny, but the youngest detrital northwest-flowing streams, reflecting a local proximal source on the southeast zircon in the lower Permian Proctor sample is 364 Ma (sample WV-1-PR, Fig. 3), (Osborne, 1988, 1991). Two samples represent the Middle Pennsylvanian: the within the age range of the Acadian orogeny. stratigraphically highest preserved sandstone (Atokan Cross Mountain For- mation) in the southern part of the clastic wedge in the Appalachian basin in SUMMARY OF PROVENANCE AND MISSISSIPPIAN–PERMIAN the footwall of the leading Appalachian thrust fault in northeastern Tennessee SEDIMENT DISPERSAL IN THE APPALACHIAN FORELAND (Figs. 2, 4) (Thomas et al., 2004a), and a stratigraphically higher sandstone above the Middle Pennsylvanian (Desmoinesian) Princess No. 7 coal (sample Two major age components—Grenville and Taconic–Acadian—characterize KY-19-PR7, Figs. 2, 3). Four samples (two combined in plot 18 in Fig. 4) are the detrital-zircon populations in Mississippian to Permian sandstones in the from Upper Pennsylvanian sandstones (Conemaugh Group and Mononga- Appalachian basin. Other age contributors are relatively minor but have some hela Group; Figs. 2, 4) (Dodson, 2008) in the northwesterly prograding clas- local concentrations.

Grenville Two samples (KY-21-SG [Stony Gap] and KY-18-CB [Corbin]) have strong secondary concentrations of Superior-age grains, with peaks at 2718 and 2716 Ma Grenville-age (1300–950 Ma) detrital zircons are dominant in many sand- (Fig. 3). Because these samples are distant from the Canadian Shield and are stones and are a strong component in the others (Fig. 11). No clear indications of isolated within the recognized dispersal systems (distal Mauch Chunk–Potts- systematic lateral or vertical variations in sediment contributions from Grenville ville clastic wedge and mid-stream longitudinal system, respectively), recy- sources are evident (Figs. 3, 4). Grenville-age detrital zircons may have been cling from synrift or passive-margin sedimentary deposits is the most likely supplied from primary sources in the Appalachian basement massifs (Fig. 5), source for the Superior-age grains. Both geographically proximal and strati- from recycling of detrital zircons in Appalachian sedimentary rocks spanning graphically in succession, the samples may represent either a local source the stratigraphic succession from Iapetan synrift to Acadian synorogenic de- followed by recycling or a persistent local source along this specific part of posits (Figs. 7–10), or most likely from both primary and secondary sources. the Appalachian orogen. Other sandstones in the Mauch Chunk–Pottsville clastic wedge (Tumbling Run, Fig. 4) and in the southern part of the longitudinal system (Raccoon Mountain, Lee, Sewanee, and upper Raleigh; Fig. 4) have Taconic–Acadian minor concentrations of Superior-age grains, suggesting some continuity of sub-regional supply. The local supply for recycling might have been a concen- Detrital zircons with ages of 490–350 Ma constitute a prominent mode in tration of Superior grains in synrift sandstones (Irishtown and Rome, Fig. 7) many of the samples, but the relative abundance differs through the sample or in passive-margin sandstones, such as in the Midcontinent and Ouachita set from most dominant to completely lacking (Figs. 3, 4, 11). Taconic and Aca- margin (Midcontinent and Blakely, Fig. 8). Some Taconic (Fig. 9) and Acadian dian plutons provide primary sources of zircons with ages of 490–420 and 420– (Fig. 10) sandstones contain Superior-age grains, although none as abundant 350 Ma, respectively (Fig. 5). The Taconic and Acadian clastic wedges contain as in the Stony Gap and Corbin (Fig. 3). only very rare synorogenic zircons; however, the Acadian clastic wedge does In most of the samples, generally minor, secondary concentrations with have Taconic-age detrital zircons available for recycling (Figs. 9, 10). ages of 2000–1320 Ma correspond in age to several provinces (Trans-Hud- The distribution of detrital zircons indicates a greater proportion of Taconic– son, Penokean, Central Plains, Granite-Rhyolite) of the Laurentian craton and Acadian rocks in the Mauch Chunk–Pottsville drainage system than in the Early Canadian Shield (Fig. 1); generally, abundance of detrital grains decreases Pennsylvanian part of the Pennington-Lee system; however, Taconic–Acadian with increasing age of the province. The Grenville province includes reworked contributions increased irregularly through time in the Pennington-Lee system enclaves of some of these older rocks, providing a potential primary source. (Fig. 11). The distribution of Taconic–Acadian components also indicates that Some Iapetan synrift sediment accumulations, as well as younger Appalachian sediment (with dominant Taconic–Acadian peaks) from the transverse Mauch sedimentary rocks, contain detrital grains of these ages, providing a source for Chunk–Pottsville drainage merged into the northern upstream part of the lon- recycling. gitudinal system, and downstream variability suggests intermittent contribu- Accreted terranes of Gondwanan affinity form much of the Appalachian tions from the transverse drainages during the Early Pennsylvanian. internides, but detrital zircons from potential Gondwanan sources are rare in The Hf isotopic data support a distinction in sources of detritus for the two the foreland detritus. The Lower Pennsylvanian Lee and Sewanee sandstones clastic wedges, as well as diversion of the Mauch Chunk–Pottsville dispersal (Fig. 4) in the longitudinal system contain a few grains of Eburnian–Trans-Ama- system into the longitudinal system. Taconic–Acadian zircon grains with inter- zonian ages, suggesting an unusual minor contribution from accreted terranes

mediate (–5 to +5) εHft values are scattered through the foreland sandstones, through transverse drainage into the longitudinal drainage. Detrital zircons in but samples from the Pennington-Lee clastic wedge generally have only those the age range of 765–530 Ma are rare but are scattered throughout many of values. In contrast, samples from the Mauch Chunk–Pottsville clastic wedge the samples with no obvious trends in space or time (Figs. 3, 4). The Pan-Afri- and the longitudinal system also contain grains with more negative and more can–Brasiliano zircons cannot be distinguished on the basis of age alone from

positive εHft values, suggesting a provenance with more heterogeneous Iapetan synrift igneous zircons of the Laurentian rifted margin. Although the crustal materials than in the provenance for the Pennington-Lee clastic wedge. synrift igneous rocks are distributed along the Appalachian external basement massifs, and Gondwanan terranes form much of the Appalachian internides (Fig. 1), the general paucity of detrital zircons of these ages indicates only very Detrital Zircons in Minor Concentrations minor contributions from either. Although plutons with ages (330–270 Ma) of the Alleghanian orogeny are Many (but not all) of the samples have at least a few grains with ages of distributed along the Appalachian internides, only seven detrital grains have 2950–2530 Ma. The ultimate primary source for these grains is the Superior ages within that range (Figs. 3, 4). The lack of synorogenic grains suggests province of the Canadian Shield, which provided sediment to synrift basins either lack of unroofing or lack of integrated drainage from the internides (e.g., along the Iapetan rifted margin of Laurentia and to the passive-margin shelf. Thomas et al., 2004a). A similar lack of synorogenic grains also characterizes

sandstones in the Taconic and Acadian clastic wedges (Figs. 9, 10), suggest- Recycling ing that Appalachian clastic wedges are “one orogeny behind” in the detrital- zircon record (Thomas et al., 2004a). The distribution of zircon ages within various successive sedimentary accumulations implies multiple recycling. For example, some Iapetan synrift Other Interpretations of Provenance and Sediment Dispersal sediment accumulations contain only Grenville-age detrital zircons, whereas other synrift sedimentary deposits along the rifted margin and in a synrift intra- Previously, petrographic analyses of sandstones in the Pennington-Lee clas- cratonic graben contain detrital zircons older than 1300 Ma (Fig. 7), which pre- tic wedge were used to infer progressive unroofing of sedimentary rocks, low- to sumably were derived directly from primary sources in the Canadian Shield. medium-grade metamorphic rocks, plutons, and migmatites through the Lower The synrift rocks provide a source of recycled detrital zircons as old as the to Upper Pennsylvanian succession (Davis and Ehrlich, 1974). The petrographic Superior province (Cawood and Nemchin, 2001; Thomas et al., 2004a, 2004b). upward gradient parallels an upward increase in Taconic–Acadian detrital zir- Similarly, passive-margin sandstones along the Laurentian margin contain a cons through the Pennsylvanian in the Pennington-Lee clastic wedge (Fig. 11), range of ages of zircons from the continental interior (Fig. 8). Both the Taconic as well as an upward decrease in grains older than the Granite-Rhyolite province and Acadian clastic wedges provided a large source for recycling a wide range (Figs. 3, 4). No genetic relationship between the upward increase in metamor- of ages of detrital zircons (Figs. 9, 10). phic grade of the source rocks and the ages of detrital zircons is evident. Many previous reports on the quartz-pebble–bearing quartzarenites of APPALACHIAN SIGNATURE IN DETRITAL-ZIRCON the longitudinal system have inferred that the quartz pebbles were supplied POPULATIONS from the Canadian Shield or igneous rocks in the northern Appalachians (e.g., Siever and Potter, 1956; Heimlich et al., 1975; Edmunds et al., 1979). The new The probability plots for each of the samples (both new and previously samples from the Sharon Conglomerate (samples OH-4-SN and OH-1-SS, published), as well as various combinations of plots including a plot of all Fig. 3) in the northern part of the Appalachian longitudinal system are most analyses, show great commonality of populations (Figs. 3, 4, 11, 12). These proximal to the Canadian Shield (Figs. 1, 2). Both Sharon samples contain only data lead to a comprehensive characterization of the ages of detrital zircons a few zircon grains with ages that correspond to the older provinces (Superior, that are available to be more widely dispersed beyond the Appalachian fore- Penokean, and Central Plains) of the Canadian Shield and, instead, are domi- land, and thus provide a template of an “Appalachian signature” for recog- nated by Taconic–Acadian and Grenville ages (Fig. 3). nition of detrital-zircon populations from Appalachian sources. The primary t e & e- ville yolit conic ican– cadian r Ta A Rh Granit Superior nokean & Gren asiliano & ntral Plains Eburnian Pe ans-Hudson an-Af Alleghanian Br P Ce Tr Iapetan synrif ans-Amazonian 1066 Ma Tr Figure 12. Composite relative age-probability plot of all results of U-Pb analyses

1165 Ma from the late Paleozoic succession in the Appalachian foreland (compiled from data in Figs. 3 and 4) to illustrate the “Appala- chian signature” of detrital-zircon populations. Vertical colored bands represent

455 Ma the age ranges of potential provenance 422 Ma 396 Ma

Probability provinces in the Appalachians and North American craton. N—number of separate

1325 Ma ALL (N=29, n=3564) samples; n—number of individual grain

1451 Ma analyses. 1649 Ma 609 Ma 1750 Ma 2714 Ma 545 Ma 1812 Ma 2575 Ma 1975 Ma 2111 Ma

200 400 600800 1000 1200 1400 1600 1800 2000 22002400 2600 2800 3000 3200 Detrital Zircon Age (Ma)

characteristics are (1) a general lack of grains older than 1500 Ma, (2) a domi ACKNOWLEDGMENTS nance of Grenville-age grains, (3) a paucity of grains from accreted Gond This research, including sample collecting and analyses, has been funded by National Science wanan terranes or from Iapetan synrift rocks, (4) a strong component of Foundation (NSF) award EAR-1304980. Beth Welke assisted in the field work. Dreadnaught Stubbs, a student at Ohio University, conducted the U-Pb analyses of samples OH-4-SN and OH-1-SS. Taconic and Acadian zircons, and (5) a general lack of Alleghanian-age grains All analyses were conducted at the Arizona LaserChron Center with the support of NSF award

(Fig. 12). The range of εHft values for zircons older than 900 Ma is consis- EAR-1338583. A constructive review of the manuscript by Tim Lawton for Geosphere is gratefully acknowledged. tent with values from Laurentian craton provinces. The εHft values for Taconic and Acadian zircons range from positive to negative and indicate variations in the provenance. The longitudinal system may have diverted much of the REFERENCES CITED detritus along strike of the Appalachian foreland, limiting dispersal onto the Aleinikoff, J.N., Moench, R.H., and Lyons, J.B., 1985, Carboniferous U-Pb age of the Sebago craton, during the Early Pennsylvanian. At other times, sediment may have batholith, southwestern Maine: Metamorphic and tectonic implications: Geological Society of America Bulletin, v. 96, p. 990–996, doi:10 .1130 /0016 -7606 (1985)96 <990: CUAOTS>2 .0 .CO;2 . been transported across the Appalachian foreland and onto the craton, and Aleinikoff, J.N., Horton, J.W., Jr., Drake, A.A., Jr., and Fanning, C.M., 2002, SHRIMP and conven- the recognition of Appalachian-derived detritus can be based on the distribu- tional U-Pb ages of Ordovician granites and tonalites in the central Appalachian Piedmont: tion shown in Figure 12. Implications for Paleozoic tectonic events: American Journal of Science, v. 302, p. 50–75, doi:10.2475/ajs.302.1.50. Allen, J.S., 2009, Paleogeographic reconstruction of the St. Lawrence promontory, western New- foundland [Ph.D. thesis]: Lexington, University of Kentucky, 288 p. 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Bartholomew, M.J., and Hatcher, R.D., Jr., 2010, The Grenville orogenic cycle of southern Lau- land uniformly indicate a primary provenance in the “Alleghanian orogen” rentia: Unraveling sutures, rifts, and shear zones as potential piercing points for Amazonia: (summary in Thomas, in Hatcher et al., 1989b); however, the Alleghanian oro- Journal of South American Earth Sciences, v. 29, p. 4–20, doi:10.1016/j.jsames.2009.08.007. gen is a complex composite of disparate elements, including Grenville-age Bayona, G., and Thomas, W.A., 2006, Influence of pre-existing plate-margin structures on fore- crystalline rocks in Appalachian basement massifs, Iapetan synrift igneous deep filling: Insights from the Taconian (Blountian) clastic wedge, southeastern USA: Sedi- mentary Geology, v. 191, p. 115–133, doi:10.1016/j.sedgeo.2006.02.001. rocks and sedimentary deposits, passive-margin sandstone and carbonate Becker, T.P., Thomas, W.A., Samson, S.D., and Gehrels, G.E., 2005, Detrital zircon evidence of succession, Taconic and Acadian synorogenic igneous rocks and accreted ter- Laurentian crustal dominance in the lower Pennsylvanian deposits of the Alleghanian clas- ranes, Taconic and Acadian clastic wedges, and Alleghanian synorogenic ig- tic wedge in eastern North America: Sedimentary Geology, v. 182, p. 59–86, doi:10 .1016/j .sedgeo.2005.07.014. neous rocks and accreted terranes. 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