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Comparison of the Elemental Geochemistry of the Arkansas Novaculite and the Boone Chert in Their Type Regions, Arkansas J Journal of the Arkansas Academy of Science Volume 70 Article 31 2016 Comparison of the Elemental Geochemistry of the Arkansas Novaculite and the Boone Chert in their Type Regions, Arkansas J. Philbrick University of Arkansas, Fayetteville, [email protected] E. Pollock University of Arkansas, Fayetteville A. Potra University of Arkansas, Fayetteville Follow this and additional works at: http://scholarworks.uark.edu/jaas Part of the Geochemistry Commons, and the Geology Commons Recommended Citation Philbrick, J.; Pollock, E.; and Potra, A. (2016) "Comparison of the Elemental Geochemistry of the Arkansas Novaculite and the Boone Chert in their Type Regions, Arkansas," Journal of the Arkansas Academy of Science: Vol. 70 , Article 31. Available at: http://scholarworks.uark.edu/jaas/vol70/iss1/31 This article is available for use under the Creative Commons license: Attribution-NoDerivatives 4.0 International (CC BY-ND 4.0). Users are able to read, download, copy, print, distribute, search, link to the full texts of these articles, or use them for any other lawful purpose, without asking prior permission from the publisher or the author. This Article is brought to you for free and open access by ScholarWorks@UARK. It has been accepted for inclusion in Journal of the Arkansas Academy of Science by an authorized editor of ScholarWorks@UARK. For more information, please contact [email protected], [email protected], [email protected]. Journal of the Arkansas Academy of Science, Vol. 70 [2016], Art. 31 Comparison of the Elemental Geochemistry of the Arkansas Novaculite and the Boone Chert in their Type Regions, Arkansas J. Philbrick*, E. Pollock, and A. Potra Department of Geosciences, University of Arkansas, Fayetteville, Ar 72701 *Correspondence: [email protected] Running Title: Elemental Geochemistry of the Arkansas Novaculite and the Boone Chert in their Type Regions, Arkansas Abstract possibly even Silurian (Lowe 1985), and continued through the Kinderhookian Series, Early Mississippian. The name Arkansas Novaculite was proposed by It is bounded stratigraphically by gradational contacts A.H. Purdue, 1909 to replace the name Arkansas Stone between thick shale intervals referred to the Missouri assigned by L. S. Griswold, 1892, but deemed too Mountain Shale and Stanley Group at the base and top, generic, to an interval of Early Devonian-Early respectively. The Arkansas Novaculite has been Mississippian, very fine-grained, even textured, divided into numerous named members and siliceous sedimentary rock famous for use as submembers (Miser and Purdue 1929), but regional whetstones. The interval is exposed along the margins application of that nomenclature is questionable. This of the Benton Uplift, south flank of the Ouachita study examines the major and trace elements of Mountains, west-central Arkansas, where it reaches a informal lower, middle, and upper members of the maximum thickness of 243.8 m (800 ft). The Arkansas formation, and did not differentiate between novaculite Novaculite comprises informal lower and upper and chert. All Arkansas Novaculite samples were members characterized by massive beds of nearly pure taken from the well-known Caddo Gap roadcut, novaculite, separated by a shale-bearing middle located on the southern flank of the Benton Uplift, the member that spans the Devonian-Mississippian structural core of the Ouachita Mountains in east- boundary. The formation represents deep water central Arkansas. deposition below carbonate compensation depths, in The source of the silica for both the Arkansas contrast to contemporaneous chert-bearing intervals, Novaculite and Boone chert has generated considerable such as the Early Mississippian Boone Formation in debate, although there has been little comparison of the the southern Ozarks, with chert formed in shallower two intervals. Most studies of the Novaculite (Sholes marine conditions, or as a replacement of associated and McBride 1975 is typical), and Boone and other limestone beds. chert-bearing intervals (see Hesse 1990 for a review) Source of the prodigious quantities of silica cite altered siliceous bioclastic remains, commonly forming the Arkansas Novaculite has been sponge spicules, as the silica source. However, other controversial. Geochemical analyses, using both EDX proposed origins for the Novaculite silica include and trace element analysis, were performed using mass simultaneous dissolution of limestone and precipitation spectrometry and have identified a significant of silica (Rutley 1894, Derby and Banner 1898, contribution by both aluminum and potassium, which Correns 1950), volcanic ash deposited in a sediment- would seem to eliminate a biogenic origin and favor a starved basin (Goldstein and Hendricks 1953), and volcanic source, perhaps related to an island arc system hydrothermal alteration of quartz sandstone (Owen that formed during the Ouachita Orogeny as Laurasia 1860, Comstock 1888). Tarr (1926) hypothesized collided with Gondwana. Trace element analysis also direct precipitation of silica as a colloidal sol derived suggests that the Arkansas Novaculite and the chert in from terrestrial erosion and transported to marine the Boone Formation may have both been formed from environments by rivers and streams for the Boone and the same volcanic source. other midcontinent chert. Introduction Geologic Setting Deposition of the Arkansas Novaculite, named by Paleozoic Area of Arkansas Purdue (1909), began during the Early Devonian, The Paleozoic area of Arkansas comprises three Journal of the Arkansas Academy of Science, Vol. 70, 2016 184 Published by Arkansas Academy of Science, 2016 184 Journal of the Arkansas Academy of Science, Vol. 70 [2016], Art. 31 Elemental Geochemistry of the Arkansas Novaculite and the Boone Chert in their Type Regions, Arkansas north vergent, excluding the cores of the Benton and Broken Bow Uplifts, and forms the southern margin of the Arkoma foreland basin (Arbenz 1989). Strata forming the Ouachita Mountains are dominated by deep-water facies, beginning as a starved basin from the Late Cambrian through the Early Mississippian followed by flysch sedimentation characterizing the Upper Mississippian through Middle Pennsylvanian (Arbenz 1989). The structure is the result of a collisional-subductional orogeny between Laurasia and Gondwana during the late Paleozoic era (Lowe 1975). Lithostratigraphy and Sequence Stratigraphy Tri-State Area Figure 1. Geologic Provinces of Tri-State area Ouachita Mountains. (Modified from Manger et al. 1988) This study focuses on the Lower Mississippian transgressive-regressive sequence represented by the St. Joe (Hopkins 1893) and Boone (Branner 1891) geologic provinces, from north to south: the south Formations in northern Arkansas, particularly flank of the Ozark Dome, Arkoma Basin and Ouachita peneontemporaneous chert in the lower Boone. This Mountain orogenic belt (Figure 1). The Ozark Dome is succession reflects transportation of carbonates sourced a broad, asymmetrical, cratonic uplift cored by from the Burlington Shelf, in what is now Missouri, Precambrian granite and rhyolite, with Upper which were deposited frequently as condensed Cambrian to Middle Pennsylvanian strata dipping intervals down ramp in northern Arkansas. This ramp radially away from the core area. The area lacks developed extensively along the southern margin of the structural complexity, compared to the Arkoma Basin North American Craton. The names St. Joe and Boone and Ouachita Mountains. A series of in echelon were taken from exposures in northern Arkansas and normal faults striking northeast-southwest and are the oldest, valid lithostratigraphic designations for downthrown to the southeast extends across the their respective intervals. The name St. Joe was southern Ozarks, and the regional dip averages only 19′ proposed (Hopkins 1893) as the basal, chert-free (Chinn and Konig 1973). Three broad plateau surfaces limestone member of the thicker, potentially >121.9m reflect periodic epeirogenic uplifts. From oldest and (400ft), chert-bearing Boone Formation (Giles 1935). lowest elevation, these are the Salem, Springfield, and The Lower Mississippian St. Joe-Boone interval Boston Mountains Plateaus. The Salem Plateau represents a single, third-order, transgressive- comprises Lower Ordovician limestones and dolomites regressive, eustatic cycle. It is a portion of the first- with the largest aerial extent in the region. The order Kaskaskia sequence recognized by Sloss (1963) Springfield Plateau forms the Eureka Springs that extended from the Early Devonian to the Escarpment, and is capped by limestone and chert of Mississippian-Pennsylvanian boundary, and has been the Lower Mississippian St. Joe Limestone and Boone subdivided into second-order Kaskaskia I and Formation. The Boston Mountain Escarpment and its Kaskaskia II Cycles (Witzke and Bunker 1996). The Plateau are the youngest and highest surface in the Kaskaskia I second-order cycle began in the Early Paleozoic area of Arkansas formed by Upper Devonian and extended to the Devonian-Mississippian Mississippian through Middle Pennsylvanian (Atokan) boundary, while the Kaskaskia II second-order cycle strata. encompassed the entire Mississippian. The Early The Ouachita Mountains are an east-west trending Mississippian third-order cycle includes the anticlinorium of Paleozoic rocks extending across Kinderhookian-Osagean interval (Witzke and Bunker west-central Arkansas into southeast Oklahoma. The 1996), which comprises the St. Joe-Boone carbonates Ouachita
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