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Geology of the Hollins 1:24,000 Quadrangle, Alabama

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Geology of the Hollins 1:24,000 Quadrangle, Alabama GEOLOGY OF THE HOLLINS 1:24,000 QUADRANGLE, ALABAMA By David T. Allison, Jacob Grove, and Conner Antosz LOCATION The Hollins, Alabama, USGS 7½ minute quadrangle is located includes portions of southwest Clay County, northern Coosa, and southeast Talladega counties in the Appalachian Piedmont physiographic province. The topography consists of gently rolling hills, with sharp rugged ridges and valleys trending northeast-southwest. Major drainage in the quadrangle is dendritic, with most secondary streams feeding into Hatchet Creek, which drains southwestward through the southeast quadrant of the quadrangle. In the northwest quadrant of the quadrangle minor creeks feed the southwest trending Weogufka Creek. Elevations range from 546 feet (166 meters) on Hatchet Creek at the southeastern border, to 1265 feet (386 meters) at Locust Mountain in the central portion of the quadrangle. Numerous ridge crests throughout the area reach an elevation of 1000 feet (305 meters). The area is heavily wooded and rural. Cleared land is mostly pasture land. The quadrangle is traversed southeast to northwest by US Highway 280, and north to south by US Highway 231. Hollins (pop. 585) and Stewartville (pop. 1765) are the only incorporated towns in the quadrangle. GEOLOGIC SETTING The Hollins Quadrangle is within the northern Alabama Piedmont of the southern Appalachian orogenic belt and contains rocks of three separate fault blocks: a) the Talladega slate belt of the western Blue Ridge tectonic belt, b) the Coosa block, and c) the Tallapoosa block (Tull, 1978). The latter two fault blocks form part of the eastern Blue Ridge tectonic belt. The Talladega belt on the Hollins Quadrangle occurs as a roughly triangular polygon in the northwest quadrant of the quadrangle, with internal stratigraphy repeated by a thrust fault duplex trending along the Appalachian trend. The Coosa block extends southeast from the Hollins Thrust fault in the center of the quadrangle, to the Goodwater Fault in the southeast quadrant of the quadrangle. The Tallapoosa block occupies the southeastern third of the quadrangle southeast of the Goodwater Fault. Low grade metasedimentary and metavolcanic rocks of the Talladega belt within the quadrangle range in age between Lower Devonian and Lowermost Mississippian (?) (Butts, 1926; Tull and others, 1988; Gastaldo and others, 1993), 1 whereas medium and high grade metasedimentary and metavolcanic rocks of the Coosa and Tallapoosa blocks are considered to be Neoproterozoic in age (Tull, 1978). Granitic intrusive rocks in the Coosa and Tallapoosa fault blocks range in age from Cambrian to Devonian (Russell, 1978). The Talladega belt contains stratigraphy linked to the Laurentian cover rocks of ancient North America, whereas rocks of the Coosa and Tallapoosa blocks cannot be stratigraphically linked to Laurentia and constitute part of the eastern Blue Ridge composite suspect terrane (Jefferson Terrane of Horton and others, 1991). This composite terrane may include parts of the Laurentian outer margin cover sequence, as well as accreted components of accretionary prism, including terranes with ophiolitic and island arc affinity. Major structures in the quadrangle include: a) the Hollins Line thrust fault (Tull, 1978, 1994, 1995 a, b) separating the Talladega belt in the footwall from the Coosa block in the hanging-wall, b) the Goodwater fault (Tull,1978; Tull and others, 1985; Drummond, 1986), separating the Coosa and Tallapoosa blocks, and c) the southern limb of the F4 Millerville antiform, a regional cross fold that folds the following features: thrust sheets in the eastern Appalachian foreland, the Talladega belt, the Hollins Line fault, and the Coosa block (Plate 1). Mesoscopic fold phases and mesoscopic fabrics that correlate to deformation events D1 through D5 (Tull, 1978) are observed in all rock units in the quadrangle. PREVIOUS INVESTIGATIONS William F. Prouty laid the groundwork for future studies in this region with his pioneering work on the geology of Clay County (Prouty, 1923). Few Appalachian studies of this period rival Prouty’s work in terms of detail, accuracy, and insightfulness. The geology of the Hollins Quadrangle was described in field trip guidebooks and associated field stops published by the Alabama Geological Society (Neathery and Tull, 1975; Tull and Stow, 1979), and in an open file report to the Geological Survey of Alabama (Tull, 1976). Studies focusing on the Hillabee Greenstone in the quadrangle include work by Tull and others (1978), and Tull and Stow (1980), and thesis work by Long (1981) and Durham (1993). The southernmost part on the quadrangle borders on an area included in a study by Drummond and others (1994). ACKNOWLEDGMENTS The authors have worked closely over the years with several other geologists in researching the geology of the Hollins Quadrangle and the discussions and visits to the quadrangle with these individuals are gratefully acknowledged in adding to our understanding of this area. Thornton Neathery introduced the geology of the Alabama Piedmont to the geological community and his insight has been invaluable to multiple generations of geologists in identifying key problems for research in the region. James Tull, Lamar Long and Steve Stow conducted the first generation of detailed structural and geochemical studies of the northern Alabama Piedmont, particularly with respect to the Hillabee Greenstone and Paleozoic granitic rocks. The authors would also like to thank 2 the Jesse Edmondson of Charge Minerals, LLC, for logistical help, structural data from leased properties, aid in gaining access to properties, and for crystalline graphite analyses data. STRATIGRAPHY STRATIGRAPHIC NOMENCLATURE The following outline is a brief summary of the stratigraphic nomenclature and known age relationships for units related to the geology of the Hollins Quadrangle: Map Symbol (Plates 1 and 2) Unit Age rg Rockford-type Granitoids Devonian(?) hgs Hillabee Greenstone Devonian(?) hd Hillabee Metadacite Devonian(?) Dtjc/Dtes Jemison Chert/Erin Slate Devonian S-Dtbr Butting Ram Sandstone Siluro-Devonian S-Dtld Lay Dam undiff. Siluro-Devonian wec Wedowee Group Cragford Neoproterozoic (?) lithology weh Wedowee Group Neoproterozoic (?) Hackneyville lithology hc Hatchet Creek Group undiff. Neoproterozoic (?) hcg Hatchet Creek Group Neoproterozoic (?) metagreywacke hf Higgins Ferry Group undiff. Neoproterozoic (?) hfgr Higgins Ferry Group Neoproterozoic (?) graphitic schist hfmg Higgins Ferry Group Neoproterozoic (?) metagreywacke hfgq Higgins Ferry Group Neoproterozoic (?) graphitic quartz hfa Higgins Ferry Group Neoproterozoic (?) amphibolite ASHLAND SUPERGROUP Stratigraphic terminology in this region of complex geology has evolved over time as more structural and stratigraphic work and interpretations based upon this work have occurred. The “Ashland Series” was first described in Clay County by Prouty (1923) to include all of the rocks between the Hollins Line fault (then believed to be an extension of the Whitestone fault of north Georgia) and what is now mapped as the trace of the Goodwater fault, with the exception of a 3 narrow strip of rocks to the southeast, which Prouty referred to as “Altered Talladega”. Later, Butts (1926) referred to these two sequences in this area as the “Ashland mica schist” and the “Wedowee formation”. Neathery and Reynolds (1973) referred to both of these sequences as the Wedowee Group. Southeast of the trace of the Goodwater fault, in the Millerville Quadrangle, Prouty mapped the sequence as part of the “Ashland Series”, whereas Butts referred to it as “Ashland mica schist” and Neathery and Reynolds (1973) mapped it as Wedowee Group. Neathery (1975) and Tull (1978) recognized two lithologically distinct sequences in the northern third of the Millerville Quadrangle in rocks that Prouty (1923) had mapped as his “Ashland Series”, and Butts (1926) mapped as “Ashland mica schist”. Within these sequences formation level units can also be differentiated, so Tull (1978) elevated the Ashland to supergroup status (Ashland Supergroup), and subdivided it into a structurally lower (northwestern) sequence and a structurally upper (southeastern) sequence. At the latitude of the Millerville Quadrangle (northeast of Hollins quadrangle, 33° 11′ N), the Ashland Supergroup is folded into the regionally developed Millerville cross-antiform, which is decapitated down plunge to the east by the Goodwater fault. The south limb of the Millerville cross-antiform can be observed by tracing the curved contact of the Hollins Thrust in the northeast portion of the Hollins quadrangle (Plates 1 and 2). The Millerville cross-fold separates the Ashland Supergroup into a northeastern and a southwestern salient. In the southwestern salient, Neathery (1975) referred to the structurally lower sequence as the Higgins Ferry Formation and to the equivalent sequence in the northeastern salient as the Poe Bridge Mountain Formation. He referred to the structurally upper sequence in the southwestern salient as the Hatchet Creek Group, and that in the northeastern salient as the Mad Indian Group. Tull (1978) correlated the Higgins Ferry and Poe Bridge Mountain Formations and the Hatchet Creek and Mad Indian Groups across the Millerville antiform, upgraded the Higgins Ferry and Poe Bridge Mountain Formations to group status, and combined these two sets of equivalent groups into the Ashland Supergroup. In the Hollins Quadrangle the Ashland Supergroup is represented by the Higgins Ferry Group and the Hatchet Creek Group
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