U-Pb Detrital Zircon Geochronology of the Upper Paleocene to Lower Eocene Wilcox Group, East-Central Texas GEOSPHERE; V

Research Paper

GEOSPHERE U-Pb detrital zircon geochronology of the Upper Paleocene to Lower Eocene Wilcox Group, east-central Texas GEOSPHERE; v. 12, no. 5 Preston J. Wahl*, Thomas E. Yancey, Michael C. Pope, Brent V. Miller, and Walter B. Ayers Department of Geology and Geophysics, Texas A&M University, College Station, Texas 77843, USA doi:10.1130/GES01313.1

12 figures; 4 supplemental files ABSTRACT INTRODUCTION

CORRESPONDENCE: pjwahlgeo@gmail.com Arrival of Laramide uplift sediments to the Texas Gulf Coastal Plain and Upper Paleocene and Lower Eocene strata comprising the Wilcox Group northwestern Gulf of Mexico during the early Paleogene is recorded in strata and overlying Claiborne Group occur along the Gulf Coastal Plain from south- CITATION: Wahl, P.J., Yancey, T.E., Pope, M.C., of the Wilcox Group as a significant increase in sediment accumulation and western Texas to central Alabama. Wilcox Group and Claiborne Group strata Miller, B.V., and Ayers, W.B., 2016, U-Pb detrital zircon geochronology of the Upper Paleocene to with the appearance of 65–52 Ma detrital zircons that correspond with the are an important economic resource in the Texas Gulf Coastal Plain and north- Lower Eocene Wilcox Group, east-central Texas: timing of late Laramide uplift. New U-Pb dating of detrital zircons by laser western Gulf of Mexico. Both groups contain important aquifers (Thorkildsen Geosphere, v. 12, no. 5, p. 1517–1531, doi:10 .1130 ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) for and Price, 1991), and the east-central Texas region contains a significant per- /GES01313.1. samples obtained from the Lower Paleocene Tehuacana Member through centage of total Texas Wilcox Group lignite coal reserves (Kaiser et al., 1980). the Lower Eocene Queen City Formation in east-central Texas identifies the Additionally, deep-water amalgamated channel systems and associated de- Received 8 January 2016 Revision received 31 May 2016 Hooper Formation of the Wilcox Group as the oldest stratigraphic unit to posits of the Wilcox Group equivalent are important hydrocarbon targets in Accepted 28 July 2016 contain 65–52 Ma ages. Late appearance of 65–52 Ma detrital zircons in the the northwestern Gulf of Mexico (Meyer et al., 2005). These resources have Published online 23 August 2016 Hooper Formation is correlated with unroofed Laramide magmatic intrusions made Paleocene and Eocene strata subject to various geologic studies, includ- or nearly syndepositional volcaniclastic sources; whereas older detrital zir- ing those related to sedimentary provenance (Hutto et al., 2009; Mackey et al., cons are inferred to be derived primarily from sedimentary cover and base- 2012). Previous U-Pb age dating of detrital zircons from Paleocene and Eocene ment rocks exposed during uplift of Laramide blocks. strata along the northwestern Gulf Coastal Plain includes areas in south Texas Stratigraphic River Sample Location DescriptionLatitude/Longitude Sampling Level System Potential source region and Gulf Coastal Plain detrital zircon data sup- (Mackey et al., 2012), east-central Texas (Hutto et al., 2009), central Louisiana Queen City Buffalo South, Rt. 79 roadcut near pond, 6 km SW 31.405461°N; base Navasota Fm of I-45 at Buffalo, Leon Co., TX 96.111382°W port a relatively similar paleodrainage area and sediment sources for east- (Craddock and Kylander-Clark, 2013), and a regional study extending from Cart Path on Pine Forest golf course, 90 m north of 30.073912°N; Carrizo Fm fluvial base Colorado River, 4.5 km from Rts.21-71 intersection, Colorado 97.281754°W Tahitian Village, Bastrop Co., TX central Texas Tehuacana Member to Carrizo Formation and central Louisiana southwestern Texas to central Alabama (Blum and Pecha, 2014). This study ad- Big Brown mine, NE end, N side Rt. 2570, west Calvert Bluff 31.838566°N; mid side Trinity River, 16 km NE of Fairfield, Freestone Trinity Fm 96.050466°W Co., TX Wilcox Group data, and for east-central Texas Queen City Formation and vances efforts to further characterize these strata along the Gulf Coastal Plain

Black Shoals, Brazos River, 0.4 km SW of Rt. 979 Calvert Bluff 30.976752°N; base bridge, east side of river, 8.4 km due west of Brazos Fm 96.760524°W central Louisiana middle-upper Claiborne Group data. South Texas Wilcox by providing U-Pb age data for 12 sandstone samples from closely spaced Calvert, Robertson Co., TX

Thornton quarry, south side Rt. 1246, 6 km SE of 31.386536°N; Simsboro Fm high Navasota Group data contrast with data from these samples and support a differ- stratigraphic horizons in east-central Texas. Samples were obtained from lo- Thornton, Limestone Co., TX 96.509098°W

Kosse mine (U. S. Silica), east side of Rt. 2749, 1.3 ent paleodrainage area and sediment sources for the south Texas region. cations between Bastrop and Freestone Counties of east-central Texas where 31.295041°N; Simsboro Fm top km north of Rts.7 and 2749 intersection, 11.6 km Navasota 96.508852°W ESE of Kosse, Limestone Co., TX We propose that headwaters sourced from southeastern Wyoming to the strata crop out in and in close proximity to the Colorado, Brazos, and Trinity Luminant pit, 0.6 km west of Rt. 2749, 1.1 km NW 31.314138°N; Simsboro Fm mid of Kosse U.S. Silica mine plant, 10.8 km due east Navasota 96.516782°W of Kosse, Limestone Co., TX southern Rocky Mountain region delivered sediments to east-central Texas River Valleys (Figs. 1 and 2), all of which are located in the Houston embay- Rt. 14 roadcut, east side of road, 160 m SW of Rt. 31.223429°N.; Simsboro Fm low 276 intersection to the east, 9.5 km SW of Kosse, Brazos 96.649808°W Limestone Co., TX and central Louisiana during the Paleocene to Middle Eocene. Pronounced ment structural basin. Sandstone samples are from the Lower Paleocene Mesoproterozoic and Neoproterozoic detrital zircons in the lower Claiborne Tehuacana Member at the top of the Kincaid Formation of the Midway Group 1Supplemental Item 1. East-central Texas sample Group of east-central Texas and the middle-upper Claiborne Group of cen- to the Lower Eocene Queen City Formation of the lower Claiborne Group. location details. Please visit http://dx .doi .org /10 1 .1130/GES01313 .S1 or the full-text article on www tral Louisiana are attributed to new or unroofed recycled sediments with Sample location details are available in Supplemental Item 1. .gsapubs.org to view Supplemental Item 1. Grenvillian age detrital zircons incorporated from the Ouachita region and Sediment delivery to the Texas Gulf Coastal Plain and northwestern Gulf of other proximal locations in the preexisting paleodrainage area. The inferred Mexico during the early Paleogene is characterized by a substantial increase of paleodrainage area for east-central Texas and central Louisiana includes clastic sediment volume during the Late Paleocene, followed by an overall de- most of the Rocky Mountain Laramide uplift blocks, has a southern bound- cline of sediment delivery until the Late Eocene (Galloway and Williams, 1991; ary separating it from a south Texas paleodrainage, and an eastern boundary Galloway et al., 2011). Wilcox Group and lower Claiborne Group sediments roughly coincident with the Mississippi embayment, which separates it from were deposited during a phase of clastic sediment delivery representing the Appalachian Mountains drainages. first and greatest Paleogene cycle of tectonic-influenced deposition (Winker, For permission to copy, contact Copyright 1982). This phase corresponds with timing of late Laramide orogenesis (Cather Permissions, GSA, or [email protected]. *Current address: 6900 Lake Woodlands Drive, #1111, The Woodlands, Texas 77382, USA and Chapin, 1990; Lawton, 2008) and continued development of the Western

GEOSPHERE | Volume 12 | Number 5 Wahl et al. | U-Pb detrital zircon geochronology of the Wilcox Group Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/12/5/1517/3336567/1517.pdf 1517 by guest on 29 September 2021 Research Paper

Rusk 102°W 100°W Hill Navarro Cherokee Bosque 5 36°N

98°W 96°W Waco 34°N 94°W

1 4 7 Houston 106°W 104°W Coryell 4 Leon 32°N 3 4 4 Falls Trinity Robertso Bell 3 n 30°N 5 Madison Polk Walker Milam 28°N B/CS ~500 km Williams Grimes on J acinto 26°N Burleson Austin Lee Liberty Lower and Middle Bastrop Washington Claiborne Group 2 Wilcox and 6 Fayette Austin Harris Midway Groups Houston Sample Location N Caldwell Fort Bend ~50 km Gonzales

Figure 1. Location of east-central Texas samples collected from areas between the Trinity and Colorado Rivers. County names are listed, and major cities are indicated by black squares. B/CS— Bryan/College Station. Blue outlines indicate major rivers. Bold black lines and shield symbols denote major interstate highways (I-10, I-35, and I-45). Extent of Midway Group, Wilcox Group, and Claiborne Group after Stoeser et al. (2005). Sample location numbers: 1—Tehuacana Member; 2—Seguin Formation; 3—Hooper Formation; 4—Simsboro Formation; 5—Calvert Bluff Formation; 6—Carrizo Formation; 7—Queen City Formation.

Cordillera (DeCelles, 2004). Extended sediment deposition on the margins of cox Group strata reported similar young detrital zircon ages (62–54 Ma) from the Gulf of Mexico resulted in an overall transition from open marine shelf the Mississippi embayment to south-central Texas (Blum and Pecha, 2014). settings during the Early Paleocene to nonmarine settings by the Oligocene, However, much of these data in east-central Texas are derived from undiffer- modulated by variation of sediment supply, subsidence, and eustatic sea level entiated Wilcox Group strata, with the Simsboro Formation being the oldest (Yancey and Davidoff, 1991; Davidoff and Yancey, 1993). Shelf-margin outbuild- identified unit. Closely spaced stratigraphic age data from this study are the ing was accompanied by sediment accumulation in large fluvial and deltaic first to constrain the relative arrival time of these young detrital zircons to depositional systems (Fisher and McGowen, 1967; Edwards, 1981; Ayers and the east-central Texas region. Lewis, 1985; Galloway et al., 2000) and development of submarine canyons The Laramide orogeny (80–55 Ma) is considered to have resulted from through which sediments were transported to the deep-water Gulf of Mexico regional northeast-southwest compressional forces and crustal shortening (Hoyt, 1959; Galloway et al., 1991). New radiometric age dates from Paleocene related to flat-slab subduction of the Farallon plate beneath the North Ameri- and Lower Eocene sandstone samples deposited in shallow marine and fluvial can plate (Dickinson and Snyder, 1978; DeCelles, 2004), although other mod- settings in east-central Texas advance the initial regional work of Hutto et al. els exist (English and Johnston, 2004). This resulted in an area east of the (2009), which identified 80–53 Ma age detrital zircons in Calvert Bluff and Car- Sevier fold and thrust belt characterized by intermontane basins (Dickinson rizo Formation strata that are considered to be derived from areas affected by et al., 1988) and associated asymmetric basement-cored uplifts that character- late Laramide uplift. Analyses of additional Paleocene to Lower Eocene Wil- ize Laramide-style deformation (Dickinson and Snyder, 1978; Lawton, 2008).

Time Lithostratigraphic May et al., 2013) Rocky Mountain region. Gulf Coastal Plain samples comprise (Ma) Epoch Stage Group Formation/Member data from south Texas (Mackey et al., 2012), central Louisiana (Craddock and 46 Queen City Kylander-Clark, 2013), and east-central Texas (this study). Formation Paleocene and Eocene Texas stratigraphic nomenclature has historically Lutetian been subdivided into major transgressive and regressive successions bound 48 Reklaw by major breaks in lithology (Sellards et al., 1932; Stenzel, 1938; Hargis, 1986). Formation In east-central Texas, lower Paleogene lithostratigraphic units are the Midway, Wilcox, and Claiborne Groups. The Paleocene component of the Midway Group 50 generally consists of abundant shale with minor sandstone beds and includes in its uppermost section the Tehuacana Member of the Kincaid Formation and Eocene

Claiborne the Wills Point Formation (Gardner, 1935). These formations were deposited 52 Ypresian Carrizo Formation in an open marine setting represented by two overall shallowing-upward successions below the Wilcox Group (Kellough, 1959). The Wilcox Group contains Figure 2. Generalized east-central abundant sandstone and shale and has extensive lignite deposits. The Seguin Texas stratigraphic column (after 54 Sellards et al., 1932; Stoeser et al., Formation marks its lowermost boundary and is overlain by the Hooper, Sims- 2005; and others) with sampled boro, and the Calvert Bluff Formations (Sellards et al., 1932; Stenzel, 1938). units indicated. See Supplemental 56 Wilcox Group depositional settings range from shallow marine, estuarine, Item 1 (see footnote 1) for sample Calvert Bluff location details. Middle Calvert Bluff fluvial-deltaic, and coastal plain settings (Sellards et al., 1932; Stenzel, 1938; Formation Formation and lower Carrizo Forma- Ayers and Lewis, 1985; Yancey and Davidoff, 1991). The overlying Lower Eo- tion samples from Hutto et al. (2009). Thanetian cene Claiborne Group generally consists of interbedded sandstone and shale 58 SimsboroFm. and comprises the Carrizo, Reklaw, and Queen City Formations from base to Wilcox Hooper Formation top (Sellards et al., 1932; Eargle, 1968). These units were deposited in shallow 60 marine, shoreface, coastal plain, and interdeltaic embayment and constructive Selandian Seguin Formation deltaic settings (Sellards et al., 1932; Stenzel, 1938; Guevara and Garcia, 1972; Yancey et al., 2010). 62 Wills Point Paleocene Formation y ANALYTICAL METHODS Danian Tehuacana 64 Mbr. Sample preparation and analyses were conducted at the Department Midwa of Geology and Geophysics at Texas A&M University. Sandstone samples Kincaid Formation from each stratigraphic horizon were collected from outcrop sections after 66 Sampled Level well-weathered surfaces or surfaces potentially containing float were removed in order to avoid sample contamination. Samples were fully disaggregated, sieved, and elutriated, with the resultant sample grain size ranging between 63 Present elevation of the entire central Rockies and adjacent parts of the Great and 300 mm. Elutriated samples were oven dried for at least 12 h at 75 °C before Plains was reached concurrently during the Late Eocene (Fan et al., 2014a), and further processing. Sorted aliquots of each sample were then concentrated into basin floors attained much of their elevation during the Early Eocene to Early heavy and light mineral fractions by methylene iodide (MEI) heavy liquid sepa Oligocene (Fan et al., 2014b). To address paleodrainage and sediment sources ration. Detrital zircons were individually picked and mounted in epoxy pucks with respect to regions such as those affected by Laramide uplift, comparisons along with Peixe (Dickinson and Gehrels, 2003), 91500 (Wiedenbeck et al., are made between composite U-Pb detrital zircon age spectra from four po- 1995), and FC-1 (Paces and Miller, 1993) zircon standards and National Institute tential source regions in the western United States and northern Mexico and of Standards and Technology (NIST) 610 and 612 glass standards. Zircon stan- from three regions along the Texas and Louisiana Gulf Coastal Plain (Fig. 3). dards Peixe and 91500 were used as either primary or secondary standards for Potential source region data represent Mesozoic through Paleogene strata and respective samples depending on the limited availability of Peixe. The FC-1 zir- were compiled from previous geochronologic studies into a northeastern Mex- con standard was used only as a secondary standard, while NIST 610 and 610 ico region (Lawton et al., 2009), a southwestern region (Dickinson et al., 2009; glass standards were used for instrumental tuning purposes. Cathodolumi- Davis et al., 2010; Mauel et al., 2011; Spencer et al., 2011), and a southern (Dick- nescence (CL) and backscatter electron (BSE) imaging were done at the Texas inson and Gehrels, 2008) and northern (Fan et al., 2011; Fuentes et al., 2011; A&M University Electron Microprobe Laboratory to generate mosaic images

ME WA VT

NH ND

MA MT MA CT WY NY MN OR ID PA SD IA WI MI NV NJ

MD DE

CO OH B NE MO C SO FR KY AM IN VA

UT IL AZ KS NM OK NC TX AR SC CA TN MS AL AW OM M MH

? GA SO FL LA LU

SMA

BC EB BS PA /P A /T A CH SI DG N LFTB CO NL TM ~500 km

East-Central Texas Samples SouthTexas Wilcox Group Southern Rocky Mtn. Region Southwestern Region

Louisiana Wilcox Group Louisiana Claiborne Group Northern Rocky Mtn. Region Northeastern Mexico Region

Figure 3. Location of potential source region and Gulf Coastal Plain data in the United States and Mexico. Physiographic highs potentially influential on sediment drainage to the northwestern Gulf of Mexico are indicated in brown, with tan or dashed features indicating uncertainty of relief and/or extent. Physiographic features adapted from (Sellards et al., 1932; Budnik, 1986; DeCelles, 2004; Flowers et al., 2008; Lawton, 2008; Galloway et al., 2011 and references therein). SOB—Sevier orogenic belt; CFR—Colorado Front Range; MH—Mogollon Highlands; LFTB—Laramide fold-thrust belt; LU—Llano uplift; SMA—San Marcos arch; AWM—Amarillo-Wichita Mountains; OM—Ouachita Mountains; AM—Appalachian Mountains; EBPA/PA/TA—El Burro-Peyotes arches, Picachos arch, Tamaulipas arch; southwestern region (Dickinson et al., 2009; Davis et al., 2010; Mauel et al., 2011; Spencer et al., 2011); northeastern Mexico region (Lawton et al., 2009); northern Rocky Mountain region (Fan et al., 2011; Fuentes et al., 2011; May et al., 2013); southern Rocky Mountain region (Dickinson and Gehrels, 2008); Louisiana Wilcox Group and Claiborne Group (Craddock and Kylander- Clark, 2013); south Texas Wilcox Group (Mackey et al., 2012); east-central Texas (this study).

LA-ICP-MSAND DATA PROCESSING

LA-ICP-MS was performed in the Texas A&M University Radiogenic Isotope Geochemistry Laboratory. A previous study of LA-ICP-MS and TIMS (Thermal Ionization Mass for all grains in a respective epoxy puck. U-Pb age data were then obtained by of detrital zircon ages in individual sample horizons. Qualitative observation of Spectrometry) U-Pb zircon ages for similar sample populations reported that LA-ICP-MS was able to produce data within 2-4% (two sigma) uncertainty (Chang et al., 2006), although high-resolution laser ablation–inductively coupled plasma–mass spectrometry east-central Texas composite probability density plot peaks, peak shoulders, and limitations of the LA-ICP-MS method are included in various publications (Feng et al., 1993; Fryer et al., 1993; Chang et al. 2006). Methods for data reduction and evaluation were modeled (LA-ICP-MS), which was performed using an Element XR single-collector mass valleys allows designation of eight primary detrital zircon age ranges that were after those developed by the Radiogenic Isotope and Geochronology Laboratory(RIGL) at Washington State University (WSU) and the Arizona LaserChron Center (Gehrels et. al., 2006). spectrometer and Analyte Exite Excimer laser ablation system at the Texas used for comparative purposes. Boundaries separate age ranges with clustered Data processing Excel spreadsheets were developed by RIGL at Washington State University. High resolution LA-ICP-MS was performed using an Element XR single collector mass A&M University Radiogenic Isotope Geochemistry Laboratory. A minimum ages or where data are scattered or relatively absent, and boundary age num- spectrometer and Analyte Exite Excimer laser ablation system by Photon-Machines Inc. Software programs used during analyses included Element 3.0 and Chromium 2.1 software. A of 300 detrital zircon grains were mounted per sample, with ~150 analyses bers correspond with maximum and minimum ages of detrital zircons in each laser spot size of 29.6 µm was used during analyses. The laser ablation system was powered by an ATLex 300si laser and operated with a wavelength of 193 nm and pulses less than 4.0 performed. The respective size of zircon standards and NIST glass standards age range. These age ranges are 3217–1970 Ma, 1958–1530 Ma, 1518–1303 Ma, nanoseconds in duration. Fluence was set at ~40% (2.2-2.4 J/cm2), and grain ablation took place at a 10 Hz laser repetition rate. He (0.8 L/min) and Ar (0.9-1.1 L/min) gas carried particles of influenced the number of standards mounted in an epoxy puck. LA-ICP-MS 1293–843 Ma, 799–676 Ma, 652–265 Ma, 251–134 Ma, and 130–52 Ma. vaporized sample to the ICP detector (measured in counts per second). procedures are described in Supplemental Item 22 and were modeled after Age ranges of Precambrian detrital zircons reveal a major difference be- 2Supplemental Item 2. Description of laser ablation– those developed by the Radiogenic Isotope and Geochronology Laboratory at tween samples of younger and older strata. A stratigraphic interval containing inductively coupled plasma–mass spectrometry (LA- Washington State University (Chang et al., 2006) and the University of Arizona samples from the Tehuacana Member of the Kincaid Formation, the Wilcox ICP-MS) and data processing procedures, as well as fractionation and secondary zircon standard results LaserChron Center (Gehrels et al., 2006). Isoplot 3.0 software (Ludwig, 2003) Group, and the Carrizo Formation contains abundant detrital zircons with ages relating to data reproducibility. Please visit http://dx was used to create probability density plots, histograms, concordia plots, and between 1958 Ma and 1530 Ma. Detrital zircons in this age range comprise .doi.org/10 .1130/GES01313.S2 or the full-text article on to determine the youngest detrital zircon age for each respective sample. De- nearly 38% of all sample ages. In contrast, the Queen City Formation contains www.gsapubs.org to view Supplemental Item 2. trital zircon age data were also assessed using the Kolmogorov-Smirnov (K-S) abundant (51% of all sample ages) 1293–843 Ma age detrital zircons with mode CONCORDIA DIAGRAMS statistical test, which tests the null hypothesis that two distributions were de- peaks at 1099 Ma and 1221 Ma and the least amount (16%) of 1958–1530 Ma age A rived from the same parent population. K-S test results and Isoplot products detrital zircons. These two age ranges and a 1518–1303 Ma age range account not included in this report are available in Supplemental Item 33. for most of the Precambrian detrital zircons, with the 3217–1970 Ma age range representing a minor amount. Precambrian–Paleozoic ages (652–265 Ma) in DETRITAL ZIRCON GEOCHRONOLOGY sample age spectra are also minor, and there is a relatively consistent absence of 799–676 Ma detrital zircon ages in all samples. These minor age ranges Apparent ages, isotopic ratios, and associated 1s absolute error values from contain too few data points for use in robust determination of provenance. 206Pb/238U, 207Pb/235U, and 207Pb/206Pb data were obtained after LA-ICP-MS data The distribution of detrital zircon ages younger than 300 Ma is relatively

B processing of detrital zircons from each sandstone sample. All samples show consistent among samples (Fig. 7). There are two multi-modal detrital zircon minimal to no detrital zircon ages between 500 and 700 Ma, which provides age ranges that are populated in all samples (251–134 Ma and 130–52 Ma), but a natural break in data sets at which to place the cutoff between the 206Pb/238U few detrital zircon ages are between 150 Ma and 105 Ma. The 251–134 Ma age age (<600 Ma) and 207Pb/206Pb age (>600 Ma) as our best interpretation of the range has mode peaks at 153 Ma and 168 Ma that appear in most samples or zircon crystallization age for concordant or nearly concordant analyses. See contains a single peak with an intermediate age. The 130–52 Ma age range has Supplemental Item 44 for all radiometric age data. Of the ~150 analyses per- mode peaks at 94 Ma, 75 Ma, and 57 Ma. Only the Sequin Formation and one formed by LA-ICP-MS per sample, the number of usable detrital zircon data per Calvert Bluff Formation sample do not contain the older peak. These two sam- sample with respect to a 10% discordant age filter varied between 94 and 140 ples lacking the 94 Ma peak also have a mode peak shifted more than ±3 Ma Figure 1. Concordia diagram for sample Teh from A) 0-800 Ma with a 0-200 Ma subplot, and B) 1000-2600 Ma with a 1000-1900 Ma subplot. ages. These U-Pb age data are displayed in individual and composite probabil- from the 75 Ma peak. The youngest mode in the 130–52 Ma age range spans

3Supplemental Item 3. Concordia diagrams, normal- ity density plots for qualitative comparison. the 65–52 Ma age interval that corresponds in time with late stages of Lara- ized age distribution plots with associated histograms, Fractionation factors of primary zircon standards and ages of secondary zir- mide uplift (Dickinson et al., 1988; DeCelles, 2004). Paleocene and Early Eocene youngest detrital zircon age plots, and Kolmogorov- con standards plotted with respect to analysis date reveal that despite change ages between 65 Ma and 52 Ma comprise 19% of the 130–52 Ma age range. The Smirnov (K-S) tests. Please visit http://dx .doi .org /10 of fractionation factors, the overall relative standard deviation of secondary oldest stratigraphic occurrence of 65–52 Ma ages is in the Hooper Formation of .1130/GES01313.S3 or the full-text article on www .gsapubs.org to view Supplemental Item 3. zircon standard ages was 3.23–5.28%. This supports a similar range of uncer- the Wilcox Group. These ages are present in younger Wilcox Group samples tainty regarding the reproducibility of east-central Texas detrital zircon ages. except for two Simsboro Formation samples. They are also absent from the Sample Isotopic RaosApparent Ages Name 207Pb/235U1σ abs. err. 206Pb/238U 1σ abs. err. 1207Pb/206Pb σ abs. err. 207Pb/235U 1σ abs. err. 206Pb/238U 1σ abs. err. 207Pb/206Pb 1σ abs. err. <10 % Discordant Samples TH_7 0.094 0.006 0.013 0.000 0.005 0.003 90.83 5.32 82.39 2.55 0.00 -98.99 Further information regarding fractionation and secondary zircon standards Queen City Formation of the lower Claiborne Group. Inconsistency in occur- TH_26 0.230 0.009 0.033 0.001 0.051 0.002 209.79 7.35 206.84 3.18 243.08 74.78 TH_29 4.334 0.151 0.299 0.005 0.105 0.003 1699.79 28.38 1688.13 26.98 1714.32 48.58 TH_30 4.271 0.176 0.301 0.008 0.103 0.003 1687.80 33.26 1694.82 41.82 1679.21 49.72 relating to the relative reproducibility of detrital zircon age data are included in rence of detrital zircons in the Wilcox and Claiborne Groups may be attributed TH_31 1.847 0.074 0.178 0.003 0.075 0.002 1062.53 26.05 1058.64 18.97 1070.51 63.35 TH_33 4.368 0.168 0.295 0.007 0.107 0.003 1706.37 31.24 1665.46 35.02 1757.11 49.34 TH_34 3.114 0.115 0.247 0.005 0.091 0.003 1436.06 28.06 1422.53 27.24 1456.29 51.77 TH_35 0.081 0.005 0.013 0.000 0.045 0.003 78.74 5.04 82.66 2.95 0.00 109.46 Supplemental Item 2 (see footnote 2). to natural bias or vagaries of sample selection and preparation (Sircombe TH_36 4.374 0.201 0.295 0.010 0.108 0.003 1707.36 37.33 1665.26 50.10 1759.54 51.78 TH_38 0.164 0.008 0.022 0.001 0.054 0.002 153.86 6.79 140.11 5.20 370.85 66.31 TH_39 3.057 0.126 0.223 0.007 0.099 0.002 1421.88 31.11 1299.28 39.34 1610.28 39.59 TH_43 2.749 0.098 0.230 0.006 0.087 0.002 1341.88 26.10 1336.23 30.20 1350.60 44.91 et al., 2001; Cawood et al., 2003; Fedo et al., 2003; Vermeesch, 2004; Moecher TH_47 0.183 0.006 0.025 0.001 0.052 0.001 170.22 5.44 161.43 3.29 293.88 63.45 TH_48 3.690 0.113 0.273 0.005 0.098 0.002 1569.13 24.18 1554.84 26.53 1588.13 39.86 TH_52 3.380 0.171 0.260 0.006 0.094 0.004 1499.73 38.86 1491.88 31.92 1509.24 75.83 and Samson, 2006; Hay and Dempster, 2009; Slama and Kosler, 2012). The TH_53 3.232 0.187 0.236 0.008 0.099 0.004 1464.75 43.97 1366.15 43.52 1609.18 78.95 EAST-CENTRAL TEXAS SAMPLES TH_56 0.971 0.061 0.107 0.005 0.066 0.003 688.73 31.08 654.84 26.68 799.26 89.87 TH_57 4.134 0.218 0.297 0.008 0.101 0.004 1661.02 42.30 1675.45 41.06 1641.23 75.67 TH_58 3.847 0.198 0.282 0.007 0.099 0.004 1602.73 40.59 1601.13 36.08 1603.24 75.29 youngest detrital zircons account for just several percent of the total sample Detrital zircon U-Pb age data (n = 1297) from east-central Texas are presented set. Despite their occasional absence, the presence of detrital zircons with ages 4Supplemental Item 4. Excel files including radio in composite probability density plots representing all 12 Paleocene and Lower that approximate the depositional age of the sampled sedimentary deposit has metric age data for east-central Texas locations. Please visit http://dx .doi.org/10 .1130/GES01313.S4 Eocene sample horizons (Figs. 4 and 5). Figures 6 and 7 reveal the distribution importance in study of provenance. or the full-text article on www.gsapubs.org to view Supplemental Item 4.

(52–130) (265–652) (843–1293) (1530–1958)

(134–251) (676–799) (1303–1518) (1970–3217)

200 75 Relative Probability Figure 4. Probability density plot and asso 150 ciated histogram of composite detrital zircon age data for all 12 east-central Texas samples. Age ranges are overlain for reference. Age labels identify pronounced probability density plot peaks and valleys of each age range. n—number of ages. 100 From oldest to youngest, each consecu- 94 tive lower boundary of an age range corre- 57 sponds with its youngest respective value Number (e.g., 1970, 1530, etc.) because no data are 168 present between age ranges. 1706

50 1099 1442 1221 All samples n = 1297 222 456 130 558 2744

0 0 500 1000 1500 2000 2500 3000 3500 Age (Ma)

(52–130) (265–652) (134–251) (52–65) 50 75

40 Relative Probabilit y

Figure 5. Probability density plot and asso 30 ciated histogram of composite detrital zir- 57 con age data of all 12 east-central Texas samples for ages younger than 300 Ma. 94 Age ranges are overlain for reference. n—

Number number of ages. See Figure 4 caption for 20 86 101 age label and age range boundary details. 153 168

10 All samples n = 299 130

0 40 80 120 160 200 240 280 Age (Ma)

(52–130) (265–652) (843–1293) (1530–1958) (134–251) (676–799) (1303–1518) (1970–3217)

QC n = 140

Figure 6. Normalized probability density plots of detrital zircon age spectra for 12 sample horizons in east-central Texas. Cz n = 98 Samples are arranged vertically with respect to stratigraphic level. n—number of ages. Interpreted east-central Texas age ranges are overlain for comparison. Labels CB-BBM n = 99 included on the right-hand side of each Relative Probability plot correspond to the formation or mem- CB-BS n = 98 ber that was sampled and/or the respective sampling location identifier if multi ple samples were collected at different Si-KM n = 135 locations. Sample labels: Teh—Tehuacana Member; Se—Seguin Formation; H-PC— Si-TQ n = 110 Hooper Formation, Polecat Creek; H-DR— Hooper Formation, Dennison Ranch; Si-B—Basal Simsboro Formation, Route Si-LP n = 97 14 roadcut; Si-LP—Simsboro Formation, Luminant Pit; Si-TQ—Simsboro Forma- tion, Thornton Quarry; Si-KM—Simsboro Si-B n = 126 Formation, Kosse Mine; CB-BS—Calvert Bluff Formation, Black Shoals; CB-BBM— H-DR n = 94 Calvert Bluff Formation, Big Brown Mine; Cz—Carrizo Formation; and QC—Queen City Formation. H-PC n = 108

Se n = 95

Teh n = 97

0 500 1000 1500 2000 2500 3000 3500 Age (Ma)

GULF COASTAL PLAIN SAMPLES source of detrital zircons based on comparison of measured ages of known basement terranes is complicated by the possibility of sediment recycling, Ages of the majority of detrital zircons in the east-central Texas region where grains may be eroded, transported, and deposited numerous times in of the Gulf Coastal Plain correspond with the timing of major igneous and sites far from the original source (Eriksson et al., 2004; Dickinson et al., 2009). metamorphic events in North America, including those related to assembly To address sediment sources and paleodrainage implications, comparison of the southern and eastern Laurentian shield (Yavapai Province [1800–1720 was made between compiled detrital zircon data from potential source re- Ma]; Mazatzal Province [1720–1600 Ma]; Granite-Rhyolite Province [1550– gions in the Western Cordillera and data from the Texas and Louisiana Gulf 1350 Ma] [Bennett and DePaolo, 1987; Karlstrom and Bowring, 1988; Whit- Coastal Plain (Figs. 8–11). Composite probability density plots of the east-cen- meyer and Karlstrom, 2007 and references therein]); the Grenville Province tral Texas region include Tehuacana Member through Carrizo Formation (1300–950 Ma) (Eriksson et al., 2004; Park et al., 2010); and the Cordilleran (Teh-Cz) data based on their observed similarity. This is appropriate for the arc (<300 Ma) of the tectonically active western margin of the continent Carrizo Formation because south Texas and Louisiana stratigraphic nomen- (Tobisch et al., 1986; Busby-Spera, 1988; Dunne et al., 1998; Saleeby et al., clature include the Carrizo Formation as part of the Wilcox Group (Hargis, 2008; Gehrels et al., 2009; Miller et al., 2009; LaMaskin, 2012). Identifying the 1986; Galloway, 2008).

(52–130) (265–652) (52–65) (134–251)

QC n = 14

Cz n = 46

CB-BBM n = 36 Relative Probability Figure 7. Normalized probability density plots of detrital zircon age spectra younger CB-BS n = 12 than 300 Ma for 12 sample horizons in east-central Texas. Samples are arranged vertically with respect to stratigraphic Si-KM n = 33 level. n—number of ages. Interpreted east-central Texas age ranges are overlain for comparison. See Figure 6 caption for Si-TQ n = 22 sample label details. Si-LP n = 12

Si-B n = 45

H-DR n = 25

H-PC n = 21

Se n = 8

Teh n = 24

40 80 120 160 200 240 280 Age (Ma)

East-central Texas (Teh-Cz) and lower Claiborne Group Queen City For- Plain samples to the northeast. East-central Texas (Teh-Cz) and central Louisi- mation detrital zircon age assemblages are very similar to Wilcox Group and ana Wilcox Group data each contain a relatively similar distribution of Precam- middle-upper Claiborne Group assemblages of central Louisiana. Both areas brian ages (Figs. 8 and 9) that contrast with less pronounced 1958–1530 Ma show a distinct change between the Wilcox Group and Claiborne Group (Figs. ages in the south Texas Wilcox Group, and south Texas Wilcox Group samples 10 and 11). East-central Texas Queen City Formation and central Louisiana mid- contain a distribution of 150–105 Ma ages that is minimal to absent in cen- dle-upper Claiborne Group data both contain a less pronounced 1958–1530 Ma tral Louisiana and east-central Texas data. Additionally, a similar distribution age range and a more pronounced 1293–843 Ma age range compared to older of 130–52 Ma ages in central Louisiana and east-central Texas contrasts with samples. Apart from young (65–52 Ma) detrital zircon ages being minimal or south Texas data, which lacks a relatively pronounced 75 Ma peak. Young 65– entirely absent in these younger strata, east-central Texas and central Louisi- 52 Ma age detrital zircons with a defined 57 Ma age peak occur in east-central ana data have relatively similar 251–52 Ma age distributions. In contrast, south Texas (Teh-Cz) and central Louisiana Wilcox Group data, but they are poorly Texas Wilcox Group data are distinct compared to equivalent Gulf Coastal represented in south Texas Wilcox Group data.

(52–130) (265–652) (843–1293) (1530–1958) (134–251) (676–799) (1303–1518) (1970–3217)

n = 1160 Southwestern Region s = 14

n = 1595 Northeastern Mexico Region s = 17

Relative Probability Figure 8. Normalized composite probability density plots of detrital zircon age spectra for potential source regions and Gulf Coastal Plain locations. n—number of ages; s—number of samples. Interpreted east-central Texas age ranges are over- n!"#"$%&' = 3107" lain for comparison. Teh-Cz—Tehuacana !"#$%&#'()"*+,(-$'.(/&01ê#4516&()&71"'Northern Rocky Mtn. Region (s("#"$) = 34" Member through Carrizo Formation data. See Figure 3 for location and sample ref- n = 596 erence details. South Texas Wilcox Group, Southern Rocky Mtn. Region s = 7 Louisiana Wilcox Group, and both Rocky Mountain region composite probability n = 737 density plots were previously compiled in * * *" South Texas Wilcox Group s = 10 Craddock and Kylander-Clark (2013). *"*" *"* *" n = 251 *" Louisiana Wilcox Group s = 2

n = 1297 East-Central Texas (Teh-Cz) s = 12

0 500 1000 1500 2000 2500 3000 3500 Age (Ma)

DISCUSSION (Lawton et al., 2009; Mackey et al., 2012). This interpretation is compatible with data shown here (Figs. 8 and 9) and extends the reach of sediment drainage to Previous literature and comparison of potential source region and Gulf the south Texas Wilcox Group into northwestern Mexico. Coastal Plain data yield an interpretation of paleodrainage and inferred con- The Llano uplift and San Marcos arch (Sellards et al., 1932) in west-cen- straints during the Paleocene and Early Eocene for sediments delivered to the tral Texas define an approximate divide between fluvial systems draining northwestern Gulf of Mexico (Fig. 12). An interpreted northward Paleogene into the Texas regions, which is consistent with previously interpreted Late drainage from the McCoy Mountains Formation of southwestern Arizona Paleocene and Early Eocene fluvial pathways to northwestern Gulf of Mexico to the Colton Formation in northeastern Utah (Davis et al., 2010) defines the depocenters (Galloway et al., 2011). Further drainage limitations in the western paleodrainage extent in the southwestern United States. Previously inter- United States follow a general path along basement structures with presumed preted Late Paleocene and Early Eocene paleodrainage to south Texas infers physiographic relief from Arizona toward the Colorado Front Range and north- a paleodrainage divide that follows the approximate path of major physio- ward toward the Black Hills of South Dakota (Mackey et al., 2012). This interpre- graphic highs along the Mexico and United States border (Galloway et al., tation highlights a divide that may discount northern Rocky Mountain region 2011). Detrital zircons with 150–105 Ma ages in south Texas Wilcox Group data data as a source of east-central Texas and central Louisiana sediments. North- and the Paleogene Difunta Group that defines the northeastern Mexico source ern Rocky Mountain region data are comparable to some Gulf Coastal Plain region (Lawton et al., 2009) are considered to be sourced from the Peninsular data, but similar age components are present in regions farther south that Range Batholith and Alisitos arc of southern California and the Baja Peninsula had shorter and simpler paths to northwestern Gulf of Mexico depocenters.

(52–130) (265–652) to Yavapai-Mazatzal basement and Sevier-Laramide sedimentary basins of southwestern Wyoming and northern and eastern Colorado (Craddock and (52–65) (134–251) Kylander-Clark, 2013). This interpretation suggests separate paleodrainage

n = 576 areas for the east-central Texas and central Louisiana regions during deposi- Southwestern Region s = 14 tion of Wilcox and Claiborne Group sediments, a conclusion not supported by our data. Late Paleocene through Middle Eocene interpretations by Galloway et al. (2011) also separate east-central Texas region and central Louisiana re- n = 955 gion catchment while incorporating drainage from the interior lowlands and Northeastern Mexico Region s = 17 Appalachian Basin region, and Blum and Pecha (2014) extend paleodrainage limits to include sediments from the Cordilleran arc batholiths of California and Idaho. Based on potential source region and Gulf Coastal Plain detrital

Relative Probability zircon data, we propose a model for a relatively similar Paleocene and Early to Middle Eocene paleodrainage area between the time of upper Midway Group through lower Claiborne Group deposition in east-central Texas and Wilcox n = 1256 s = 6 and middle-upper Claiborne Group deposition in central Louisiana, and ex- Northern Rocky Mtn. Region clude sediment contribution from the Appalachian Basin region. Detrital zircon age components from each source region appear to overlap n = 126 Southern Rocky Mtn. Region s = 20 with Gulf Coastal Plain data, with Triassic to Early Eocene data being the most unique between source regions (Fig. 9). Inferences on sediment sources for some Early Cretaceous, Paleocene, and Eocene age components were limited, n = 358 as these data were not available or underrepresented in two of the four source South Texas Wilcox Group s = 10 region data sets (southwestern region and southern Rocky Mountain region). While arrival of 65–52 Ma age detrital zircons in the Hooper Formation is late relative to the timing of initial Laramide uplift-derived sediment delivery to the n = 86 Louisiana Wilcox Group s = 2 Gulf of Mexico (recorded by the increase in sediment delivery to the upper Wills Point Formation), it provides strong evidence linking Wilcox Group sediments to a Laramide uplift source. These young grains could originate from newly n = 285 East-Central Texas (Teh-Cz) unroofed Laramide magmatic intrusions in areas such as the Colorado Min- s = 11 eral Belt (Chapin, 2012) or from nearly syndepositional volcaniclastic sources produced during Laramide uplift. Older associated detrital zircons are inferred 300 0 50 100 150 200 250 to be derived primarily from sedimentary cover and basement rocks exposed Age (Ma) by uplift of Laramide blocks. We propose that east-central Texas (Teh-Cz) and central Louisiana Wilcox Group samples both had major sediment derivation Figure 9. Normalized composite probability density plots of detrital zircon age spectra younger than 300 Ma for potential source regions and Gulf Coastal Plain locations. n—number of ages; from the southern Rocky Mountain region and received additional sediment s—number of samples. Interpreted east-central Texas age ranges are overlain for comparison. from parts of northern New Mexico, the Colorado Front Range, and south- Teh-Cz—Tehuacana Member through Carrizo Formation data. See Figure 3 for location and eastern Wyoming. Major sediment derivation from the southwestern United sample reference details. South Texas Wilcox Group, Louisiana Wilcox Group, and both Rocky Mountain region composite probability density plots were previously compiled in Craddock and States and northern Mexico suggested for the south Texas Wilcox Group Kylander-Clark (2013). (Mackey et al., 2012) is consistent with comparisons between south Texas data and components of southern Rocky Mountain, southwestern, and northeastern Mexico source region data. These detrital zircon age data and interpreted Additionally, northeasterly drainage from the northern Rocky Mountains to- paleodrainage extents highlight a unique paleodrainage and sediment sources ward the Cannonball embayment during this time (Cherven and Jacobs, 1985; for the south Texas region with respect to equivalent-age Gulf Coastal Plain Galloway et al., 2011) until the Eocene (Smith et al., 2008; Smith et al., 2014) samples to the northeast. Young (65–52 Ma) ages in one south Texas Wilcox reduces the likelihood of this region as a sediment contributor. Group sample (Carrizo Formation) are attributed to sources in northern Mexico Central Louisiana Wilcox Group and middle-upper Claiborne Group paleo (McDowell et al., 2001), not the central or southern Rocky Mountains, and are drainage extents have been previously modeled after modern Mississippi also present in the Paleocene Potrerillos Formation of the Difunta Group in River catchment, attributing the majority of Louisiana Wilcox Group sediments northeastern Mexico (Lawton et al., 2009). Implications of youngest detrital

(52–130) (265–652) (843–1293) (1530–1958) (134–251) (676–799) (1303–1518) (1970–3217)

n = 140 Relative Probability Figure 10. Normalized composite probabil- Queen City Formation s = 1 ity density plots of all detrital zircon age spectra for east-central Texas (Teh-Cz), n = 430 Queen City Formation, and central Louisi Louisiana Claiborne Group s = 3 ana Wilcox Group and middle-upper Claiborne Group samples. n—number of !" ages; s—number of samples. Interpreted !"! !" !"! !" east-central Texas age ranges are overlain n = 251 for comparison. Teh-Cz—Tehuacana Mem- !" Louisiana Wilcox Group s = 2 ber through Carrizo Formation data. See Figure 3 for location and sample reference details. Louisiana Wilcox Group and Clai- n = 1297 borne Group plots taken from Craddock East-Central Texas (Teh-Cz) s = 12 and Kylander-Clark (2013).

0 500 1000 1500 2000 2500 3000 3500 Age (Ma)

zircon data obtained in east-central Texas with ages essentially the same as the depositional age of the enclosing strata are beyond the scope of the present study. These data will be incorporated into on-going work using volcanic (52–130) (265–652) ash beds and isotope dilution–thermal ionization mass spectrometry (ID-TIMS) analyses to revise the Gulf Coast Paleocene–Eocene stratigraphic framework (52–65) (134–251) (e.g., Heintz et al., 2014).

The pronounced presence of detrital zircons with 1293–843 Ma ages in n = 14 Relative Probability Queen City Formation Claiborne Group data is distinctly different from older samples. However, s = 1 similarity of age assemblages in central Louisiana Wilcox Group and east- Louisiana Claiborne Group n = 80 central Texas (Teh-Cz) data, and in east-central Texas Queen City Formation s = 3 and central Louisiana middle-upper Claiborne Group data supports largely the same paleodrainage area and sediment sources during respective times n = 86 of deposition. This is highlighted by the similar incorporation of 1293–843 Ma Louisiana Wilcox Group s = 2 age detrital zircons in the Lower Eocene Queen City Formation of the lower Claiborne Group in east-central Texas and the Middle Eocene Sparta, Cook Mountain, and Cockfield Formations of the middle-upper Claiborne Group East-Central Texas (Teh-Cz) n = 285 in central Louisiana (Fig. 11). Either the drainage basin acquired a new geo- s = 11 graphic source area at those times, or erosion uncovered and incorporated into river sediment load an older sediment source containing 1293–843 Ma age 0 50 100 150 200 250 300 detrital zircons. Grenville Province zircons are of equivalent age (1300–950 Ma) Age (Ma) to the pronounced 1293–843 Ma age range in Claiborne Group data, and zir- conium-rich (Moecher and Samson, 2006) Grenvillian basement is exposed in Figure 11. Normalized composite probability density plots of detrital zircon age spectra younger the Appalachian-Ouachita orogenic belt and associated foreland basins (Todd than 300 Ma for east-central Texas (Teh-Cz), Queen City Formation, and central Louisiana Wilcox Group and middle-upper Claiborne Group samples. n—number of ages; s—number of samples. and Folk, 1957; Gleason et al., 2002; Eriksson et al., 2004; Park et al., 2010). Interpreted east-central Texas age ranges are overlain for comparison. Teh-Cz—Tehuacana Member A shift from garnet-epidote–enriched heavy-mineral assemblages in central through Carrizo Formation data. See Figure 3 for location and sample reference details. Louisiana Louisiana Wilcox Group strata to kyanite-staurolite–enriched assemblages in Wilcox Group and Claiborne Group plots taken from Craddock and Kylander-Clark (2013). younger Claiborne Group strata has been used to support derivation of recycled Grenvillian age (1300–950 Ma) detrital zircons from the Appalachian Basin

Paleocene-Early Eocene Early-Middle Eocene Tehuacana Mbr. to Carrizo Fm. Queen City Fm. to Cockﬁeld Fm. KS OK TX AR ME TN MS WA AWM OM

ND ME MT WY VT NH LA MN OR LU ID WI SD IA MA MI SMA MA NV CT OH EB P NY A /P NJ A PA /T DE ~250 km CO ? A B NE MO MD C SO FR KY AM IN VA

UT IL AZ KS NM OK AM NC TX AR SC CA TN MS AL A OM WM ? MH

? GA SO FL LA LU ? SM A BC E B BS PA ? /P A /T A CH N SI DG LFTB CO NL TM ~500 km ?

Figure 12. Interpreted paleodrainage to the northwestern Gulf Coastal Plain and Gulf of Mexico during the Paleocene and Early to Middle Eocene. Physiographic highs potentially influential on sedi ment drainage to the northwestern Gulf of Mexico are indicated in brown, with tan or dashed features indicating uncertainty of relief and/or extent. Physiographic features adapted from Sellards et al., 1932; Budnik, 1986; DeCelles, 2004; Flowers et al., 2008; Lawton, 2008; Galloway et al., 2011 and references therein). SOB—Sevier orogenic belt; CFR—Colorado Front Range; MH—Mogollon Highlands; LFTB—Laramide fold-thrust belt; LU—Llano uplift; SMA—San Marcos arch; AWM—Amarillo-Wichita Mountains; OM—Ouachita Mountains; AM—Appalachian Mountains; EBPA/PA/TA— El Burro-Peyotes arches, Picachos arch, Tamaulipas arch. Drainage divide indicated by red dashed lines (adapted from Galloway et al., 2011; Mackey et al., 2012; Craddock and Kylander-Clark, 2013). Yellow dashed line indicates assumed maximum shoreline position during Paleocene–Eocene time (adapted from Galloway et al. [2011]). Question mark (?) denotes uncertain extent of an associated feature. Generalized routes of sediment transport to the northwestern Gulf of Mexico indicated by dashed blue lines and arrows. Map does not depict the extent of the Baja Peninsula before pre-Miocene time (Dickinson and Lawton, 2001; Lawton et al., 2009).

region (Craddock and Kylander-Clark, 2013). Enrichment of kyanite-staurolite region transported sediments down a fairway between the Llano uplift and is also noted in lower Claiborne Group strata in Bastrop and Leon Counties the Ouachita Mountains and into their respective depocenters in east-central in east-central Texas, including parts of the Carrizo Formation, the Newby Texas and central Louisiana. East-central Texas (Teh-Cz) data show close simi Member of the Reklaw Formation, and the Queen City Formation (Todd and larity with central Louisiana Wilcox Group data and support largely the same Folk, 1957; McCarley, 1981, and references therein). While the presence of paleodrainage area and sediment sources, whereas both of these data sets kyanite-staurolite–enriched samples and 1293–843 Ma detrital zircon ages may contrast with south Texas Wilcox Group data and indicate a separate overall suggest an easterly derived source component for the Queen City Formation paleodrainage area and sediment sources for this location. of east-central Texas and the middle-upper Claiborne Group of central Louisi- Close similarity of age assemblages in east-central Texas (Teh-Cz) and ana, recycled Grenvillian detrital zircons are prominent in Pennsylvanian (Glea- central Louisiana Wilcox Group data, and in east-central Texas Queen City son et al., 2007), Permian (Soreghan and Soreghan, 2013), and Cenomanian Formation and central Louisiana middle-upper Claiborne Group data sug- (Blum and Pecha, 2014) strata of Texas. They are also present in other regions gests a relatively similar Paleocene and Early-Middle Eocene paleodrainage such as in Mesozoic and Paleogene strata in parts of the Colorado Plateau area and sediment sources. The presence of pronounced Grenvillian age de- (Dickinson and Gehrels, 2008) and the northern Rocky Mountains (Fan et al., trital zircons during lower and middle-upper Claiborne Group deposition in 2011; Fuentes et al., 2011; May et al., 2013). Xu et al. (2015) show that Gren- east-central Texas and central Louisiana, respectively, is attributed to increased ville age detrital zircons deposited in Louisiana have discordant U‑Pb and or new exposure of basement or previously covered sedimentary deposits U‑Th/He ages that indicate recycling through the Colorado Plateau area be- from the Ouachita region and other proximal locations within the preexisting fore deposition in Louisiana, and Blum and Pecha (2014) attribute Grenvillian paleodrainage area. Less pronounced Grenvillian ages in east-central Texas age detrital zircons in the Cenomanian Woodbine Formation in Oklahoma and (Teh-Cz) and central Louisiana Wilcox Group data supports a lack of sediment Texas to erosion of Upper Paleozoic foreland-basin strata in the Ouachita re- input from the Appalachian Basin region. During deposition of younger Clai- gion. Although inclusion of the Appalachian Basin region in paleodrainage borne Group sediments, incorporation of sediments with abundant Grenvil- area interpretations is popular (Galloway et al., 2011; Craddock and Kylander- lian age zircons from within the preexisting paleodrainage area is a viable Clark, 2013; Blum and Pecha, 2014), the possibility of sediment sourcing due alternative to sourcing directly from the Appalachian Basin region, and may to increased or new exposure of basement or of previously covered sedimen- suggest a false paleodrainage signal from this region during the Early and tary deposits with once-easterly derived heavy-mineral assemblages is equally Middle Eocene. viable as a source of the 1293–843 Ma detrital zircons. We hypothesize that by the time of Queen City Formation deposition, central Louisiana and east- ACKNOWLEDGMENTS central Texas regions were receiving a decreased sediment load from eroded This study was made possible by the support for graduate student research provided by the Laramide uplift blocks after Reklaw transgression (Galloway and Williams, Berg-Hughes Center for Petroleum and Sedimentary Systems at Texas A&M University. Further support was provided by the South Texas Geological Society of San Antonio, Texas. Microprobe 1991; Craddock and Kylander-Clark, 2013) and an increased sediment contribu- analyses of detrital zircon samples, zircon standards, and NIST glass standards are the work of tion from the Ouachita region and other proximal locations in the preexisting Ray Guillemette, Microprobe Laboratory, Texas A&M University. 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