Geologic atlas of the Carnegie, Doverel, Eufaula South, Morris, and Hatcher, Georgia 7.5-minute quadrangles [2007]

GEOLOGIC ATLAS OF THE CARNEGIE, DOVEREL, EUFAULA SOUTH, MORRIS, AND HATCHER, GEORGIA 7.5-MINUTE QUADRANGLES
Mark D. Cocker
In cooperation with the United States Geological Survey Cooperative Agreement #06HQAG0044
DEPARTMENT OF NATURAL RESOURCES Noel Holcomb, Commissioner
ENVIRONMENTAL PROTECTION DIVISION Carol Couch, Director
WATERSHED PROTECTION BRANCH Linda MacGregor, Branch Chief
GEORGIA GEOLOGIC MAPPING PROGRAM Open File Report 07-1
Atlanta 2007

GEOLOGIC ATLAS OF THE CARNEGIE. DOVEREL, EUFAULA SOUTH, MORRIS, AND HATCHER, GEORGIA 7.5 MINUTE QUADRANGLES
(United States Geological Survey Cooperative Agreement #06HQAG0044)
ABSTRACT
As part of the United States Geological Survey's STATEMAP Project, the Georgia Geologic Mapping Program prepared five 7.5-minute quadrangle geologic maps during 2006 and 2007. The current report contains descriptions of the stratigraphic units which have been identified and mapped in the Carnegie, Doverel, Eufaula South, Morris and Hatcher quadrangles, information on aquifer recharge zones, geologic hazards, and bauxite-kaolin deposits.

CONTENTS INTRODUCTION.................................. ........ ....... ... ... ........... .. .. ......... .... ...... .......... ........................ ... ............... .. ........ .... 1
Scope of the mapping project .................................................................................................................................. 1 Methods..... ... ... ............ ... ... ..... ............ ... ......... .. .......................... ................ ........ .... .............. ......... ..... .... ......... ... ..... . 1 Previous investigations ...... ..... .. ....... ... ........ ...... ................. .. .... ...... ... .. .... ......... ... .. ... ......... ......... .... ... ................. ... .... 5 PHYSIOGRAPHY AND LAND USE .................................... ...................................... ... ...... .. .. ... .. .. ................ .......... .. ... 6 SOILS ............................................................................................................................................................................ .. 7 GENERAL GEOLOGY ................................................................................................................................................ .. 8 STRATIGRAPHY OF THE CARNEGIE. DOVEREL, EUFAULA SOUTH, MORRIS, AND HATCHER QUADRANGLES ........................... ..... ..... .... ..... .... .... ... .. ... ..... ... ... ....... .. ... ... ........ ............ .. ..... .. ..................... ....... ........... . 10 Upper Cretaceous ..................................................................................................................................................... 10
Selma Group .................,................................................................................................................................... 10 Ripley Formation (Kr) ............................ ...... ............................................................ .. .............. .. ....... .... .. .. 10 Providence Formation (Kp) ................... ......... .......... .. ............. ........... .. .. ................. .. ... .. ... ..... .... ....... ........ 11
Lower Paleocene ........ ... ... ...... .. ..................................... ........ ...... ... ..................... .. .. .. ..... ..... ... ......... ... ...... ... .......... .. 17 Midway Group ............... .. ... ... ............ ...... ... ... ..... ... .... ..... .. .... ... ... ... .... .... ...... .. .. ..... ................. .. ......................... 17 Clayton Formation (Tel) ..................... ... ...... ............... ... ........ .. ........ .... .... .......... ......... .... .. ....... .... ... ........... 17 Porters Creek Formation (Tpc) ... ....... ... ......... ... .. .... .. .... .. ........... .. .. ...... ... ............................... .. ...... ... ..... .. .. 25
Upper Paleocene to Lower Eocene ..................................................................................... ..................................... 25 Wilcox Group .... ........ .. ........ ........... ... .. .. .................... ... ... ... .... ........... .. ................ .. ....................... ........ ........ .... 25 Nanafalia Formation (Tnf) ......................................................................................................................... 25 Tuscahoma Formation (Ttu) ... ... ... .... .. ..... .... .. ... .... .. ... ... .... .. ... ...... .. .... ...... ....... .. ... .. ... ... ... ......... ...... ... ~........ 30
Lower to Middle Eocene .. .... .. ............ ... ...... ...... .. .... ................................................................................................. 32 Claiborne Group (Tcb) ...................................................................................................................................... 32
Eocene to Oligocene ..... ............... ... ...... .. .. ..... .. ............ .... .. ..... .. .... .. ..... ...... .... ......... ..... .. .. ........................................ 35 Tertiary Sediments and Residuum (Tsr)............................................................................................................ 35
Post Upper Cretaceous- pre Miocene ........... .............................. .. .......... ...... ......... .. ...... ....... .. ................. ...... ... ...... 39 K-T breccia/conglomerate (K-Tbx) ................... .......................................... ....... ........ ........... ...................... .. ... 39
Miocene ......................................................... ..... .............. .. ... ...... ... .... ........ .. ... .... ..... ... ..... .... .. .. .. ...... .................. ... .... 45 Altamaha Formation (Ta) .... .. ........... ... .. ..... .............. .. ... ..... .. ...... .... .......... .. ... ........ .... ... .. .. ....................... ........ ... 45
Quaternary................................................................................................................................................................ 59 Tertiary- Quaternary Alluvium (TQal) .. .. ... .... ..... ... ........... .............. ...... ... ........................................................ 59 Quaternary Alluvium (Qal) .................... ..... ... ... ... ......... .............. .. ..... ... .. ... ........ ..... .............. ........... ... ... .. ... ... .... 60
Alteration of primary sedimentary textures and evidence of previous groundwater movement.. ............................. 61 Correlation ofSTATEMAP map units with the 1:500000 scale Geologic Map of Georgia .................................... 61 BIOSTRATIGRAPHY.. ........ ............. ......... ............... .. ..... .... ............. ... ... ......... .... ....... ..... ......... ... .. ......... .. .... ..... .. .. ... ...... 62 STRUCTURAL GEOLOGY ....................................................................... ...... ....... .... .... .. ...... .. ..... ..... ... .......... ... .. ......... 63 ECONOMIC GEOLOGY ......... ... ......... ... ...... ................. ..... ... .. ............. .. ... ...... .. ... .... ... .. ... .. ..... .. .. ... ............ ... .. .. ... ... ...... 76 HYDROGEOLOGY .... .... .... ........ .... .. ..... .... .................. ...... ...... .. ........... ... ........ .... ........ .. ... .... .. ........ ... ... .. ... ... .. .. .. .. .......... 79 Claiborne Aquifer... .... ... .. ... .......... .. ............ .. .................. .... .. ..... ....... .......... .. .... .. .. ...... .. ..... .. ... .. .. ......... .. ........... .. .. .. ... . 79 Clayton Aquifer ........................................................................................................................................................ 79 Cretaceous Aquifers ...... .. ... .. ...... ... .... .. ....... ... .. ... ... ... ..... .. ..................... ....... ... ........ .......... ................................ ... ..... 80 GEOLOGIC HAZARDS .. ... ........ .... .. ... ... .......... ... ... ... .. ... .................. ...... ............ .. .................. .......... ........ .. ....... .... .. .. ..... 80 SUMMARY ............. ... .... ..... .. .. .... .. ... .............. .... .. ....... .... ........... .... .... ............... .. ....... .. .... ... ................. ...... ... ................ 89 REFERENCES CITED ................................................................................................................................................... 90
FIGURES 1. Location of the Lumpkin project area in relation to the most significant recharge areas................... ... ................... 2 2. Map of Georgia showing location of STATEMAP mapping and previous 1:100,000-scale Upper
Coastal Plain geologic mapping......... ....... ...... .......... ... ....... .... .. ... ........... ............ ............ ........... .. ..... .................... ... 3 3. Stratigraphy and related aquifers in or adjacent to the current map area.................................................................. 4 4. Summary descriptions of the map units in the current map area.............................................................................. 5 5. Exposure of Ripley Formation on shore of Walter F. George Reservoir ................................................................. 11 6. Cross-bedded, gravel-rich sandstone and conglomerate of the Providence Formation ............................................ 12 7. Gravel-rich sandstone and conglomerate of the Providence Formation ................................................................... 13 8. Coarse gravel-rich conglomerate unconformably cutting sandstone of the Providence Formation ......................... 13
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9. Coarse gravel-rich conglomerate unconformably cutting conglomeratic sandstone of the Providence Formation ............. ........ .... ... ..... ...... .... ....... ... .. .... ... .............. ....... ............. ..... .. ....... ... .. .. ....... .... .. ...... .. .... .. ....... ........ .. 14
10. Interbedded coarse gravel-rich conglomerate and sandstone of the Providence Formation ..................................... 14 11. Gravel-rich conglomerate of the Providence Formation .......................................................................................... 15 12. Thick, coarse gravel-rich conglomerate interbedded with kaolinitic sandstone of the Providence
Formation...................................................................................................... ........................................................... 16 13. Outcrop of Providence Formation sandstone with the eastern (right) portion stained red by iron oxide ................. 17 14. Exposure ofkarstified limestone of the Clayton Formation immediately south of the Walter F. George
Dam on the Chattahoochee River ............................................................................................................................. 18 15. Rhodolithic limestone of the Clayton Formation immediately south of the Walter F. George Dam at
Franklin Landing, AL on the Chattahoochee River ................... .. ................ ..................................... ............. .. ......... 19 16. Soft, benthic foraminifera bearing limestone of the Clayton Formation immediately south of the Walter
F. George Dam at Franklin Landing, AL on the Chattahoochee River ............... ....... ........ ..................... .. ..... ..... ... .. 19 17. Paleokarst "solution hole" filled with Gravel Creek Member sandstone of the Nanafalia Formation at
Franklin Landing, AL on the Chattahoochee River .................. ..... ....... .......... .................. ................... ... .. ........... .... 20 18. Chert residuum of the Clayton Formation ........................................................ .. ................ .. .. ................... .. ............. 21 19. Large chert boulder containing Clayton Formation fossils .......................................... .......... .. ......... .. ...................... 21 20. Nanafalia Formation sandstone overlying soft Clayton Formation clay with soft sandstone and kaolin
of the Providence Formation in lower part of gully.................................. ............................................................... 22 21 . Iron oxide and clay residuum of the Clayton Formation ................................. ......................................................... 23 22. Iron oxide pseudomorphs after calacareous fossils indicate replacement of the Clayton Formation
limestone rather than a near-surface ferricrete-type deposit. ................. ............... .. .. ................................................ 23 23 . Small remnant of residuum of iron oxide and clay of the Clayton Formation between Nanafalia
Formation sandstone on the right and Providence Formation sandstone on the left........ ....... ................................ .. 24 24. Iron oxide and clay residuum of the Clayton Formation overlying Providence Formation sandstone on
the right and underlying Nanafalia Formation sandstone on the left .. .. .... ..... ........ ..... ..... ....... ......... .. ..... ... ... ....... ..... 24 25. Conglomerate containing angular clasts of Clayton Formation chert and rounded quartz pebbles. Is this
a basal conglomerate of the Nanafalia Formation ......................... ............................. ........ ... ........ .. ......................... 26 26. Contact between overlying Nanafalia Formation sandstone and Clayton Formation clay and iron oxide
fragments .............................................................................. .................................................................................... 27 27. Cross-bedded, kaolinitic, micaceous, coarse-grained sandstone of the Nanafalia Formation .................................. 28 28. Soft, kaolinitic, micaceous fme to coarse-grained sandstone of the Nanafalia Formation. .. .. ........ ......... .... ............. 28 29. Small prospect pit or abandoned kaolin mine in the Nanafalia Formation ........................................................ ....... 29 30. Kaolin lens or bed exposed in road drainage ditch in the Nanafalia Formation .............. .. .. .. ..... ............ .......... ....... . 29 31. Kaolin clasts in upper sandstone ofthe Nanafalia Formation ......................... ..................... .. .................................. 30 32. North dipping silty clay of the Tuscahoma Formation .. .. ........ ............. ................... .. .. .. .. .. .. .. .. ...... ... .... .. ..... .. .. ......... 31 33. Deeply weathered silty clay of the Tuscahoma Formation .... .. ...... ..... .. .... .... .. ..... ...... .. .............. .. .. ... ......... ............. .. 31 34. Soft, fme-grained sandstone of the Claiborne Group ........ ........ ......... .. ... ............ ...................................... ............. .. 32 35. Soft, fme-grained sandstone of the Claiborne Group underlies more coherent, less easily eroded
Altamaha Formation sandstone .. ...... ........ .. ..... ... ... ........... ... .... .... ...... ..... .... ......... ......... ... ... ............................. ... .. .... 33 36. Gleying alteration of fine-grained sandstone ofthe Claiborne Group .................................................................... .. 33 37. Portion of silicified tree log found near Hog Creek ........................................ ......................................................... 34 38. Contact between soft sandstone of the Claiborne Group and overlying chert and clay residuum of the
Ocala Group .... ................ .. ............ .. .......... .. ...... ......... .... ............... ... ............................................................ ............ 34 39. Chert and clay residuum of the Ocala Group overlying soft sandstoneof the Claiborne Group .............. ..... ........... 35 40. Chert clast from the Tertiary Sediments and Residuum unit (Tsr) unearthered during land clearing... ... .... .... ..... .... 36 41. Brick red sandstone of the Altarnaha Formation (Ta) overlies light brown chert and clay residuum of
the Tertiary Sediments and Residuum Unit in the left, uphill side of the photo .... .... .......... .. ......... .... ... ................... 37
42. Resistant chert residuum of the Ocala Group holds up hill along dirt road ....................................................... ...... 37 43 . Intensive kaolillization of fme-grained sandstone with several "boulders" of relatively unaltered
sandstone.. ... .. .... ... .................. ... .. ... .. .. .......... ......... ........... .. .. ........ ...... .. ....... .................... ... .. ....... ... ........ .... ... .......... . 38 44. Intensive kaolillization and bleaching of fme-grained sandstone with relatively unaltered sandstone .................... . 38 45. Outcrop of conglomeratic clay (K-Tbx) in unconformable contact with cross-bedded sandstone of the
Providence Formation ...................... .................... ....... ..... ..... ...................................... ... .. .......................... ....... ....... 40 46. Heterolithic conglomerate of angular sandstone, botryoidal goethite, and rounded to subangular kaolin
clasts about 10 feet east of the previous photo and 4 to 5 feet lower in elevation. ...... ...................... .. .. .... .. ... ... ...... 40
iii

47. Botryoidal, goethite clasts common in this basal conglomerate ............................................................................... 41 48. Channel sandstone of the Nanafalia Formation down cutting into Clayton Formation clay that grades
down to conglomerate (K-Tbx) exposed in lower third if outcrop .... .............................. ........ .............................. ... 42 49. Rapidly fming upward conglomerate consisting of abundant rounded to subangular kaolin, sandstone,
and botryoidal goethite clasts in clay and sand matrix .............................................. ............................................... 43 50. Outcrop of clast-rich conglomerate approximately 0.5 miles E of the previous outcrop shown in Figs.
45-50 ... ... ......... ...... .. .. ............................... ...................... .. ....................... .......... .... .................. ............................ 44 51. Another exposure of clast rich conglomerate ................................ ................ ............................. .................. ............ 44 52. Basal sandstone of the Clayton Formation with suspended clasts of gray kaolin from the underlying
Providence Formation kaolin................................................................ ..................................................... .. ....... ..... 45 53 . Layers of ironstone pebbles are visible within the base of the Altamaha Formation. Base of hammer is
at Altarnaha - Claiborne sand contact ..... ...... .............. .. ......... ... ......... ..... ................ ................................ .... .......... .. . 47 54. Iron oxide-cemented ironstone pebbles form a layer approximately 1 foot thick .................. .... ............................ .. 48 55. Channel of the massive, brick-red, pebble-rich conglomeratic sandstone of the Altamaha Formation
cutting into reddish brown sandstone of the Providence Formation .. .. ....... ... ............... ... .... ........ .............. .. .. ... ....... 50 56. Basal cobble conglomerate of the Altamaha Formation overlying sandstone of the Claiborne Group ........ .. ......... 50 57. Channel of Altamaha Formation sandstone cut into soft sandstone of the Claiborne Group sandstone ................... 51 58. Large stream channel of Altamaha Formation cut into Oligocene-age(?) Tobacco Road Sand ............... ............ .... 51 59. Lower contact of Altamaha Formation marked by boulder conglomerate .. ......................................................... .... 52 60. Channel in Altamaha Formation marked by thin pebble bed that cuts across apparently massive
sandstone ..... ........ ...... ........ ... ... ... ... ....... ... .. ...... .. ........... ... ................ ... ..... ... ....... ........... .................... .... .. .... ........... ... 52 61. Right side of channel shown in Fig. 60 .... ...... ... ...................... .... ...................... ......... ...................... ................... ..... 53 62. Channel edge of conglomeratic sandstone of the Altamaha Formation cuts down into softer sandstone
of the Providence Formation .................................... .. ..................................... ..... .... .. .............................................. 53 63. Brick-red conglomeratic sandstone cuts several channels into underlying brown sandstone of the
Nanafalia Formation.............................................................................................. ... .... ............................................ 54 64. Basal megaclast conglomerate of the Altamaha Formation overlying soft sandstone of the Claiborne
Group ... ..... .................. .......... .. ....... .. .. ... ...... .......... ...... ........... ... .........................................,.... .... .............. ........... 54 65 . Channel of pebble-rich conglomerate of Altamaha Formation cutting underlying Nanafalia Formation
sandstone. ..... ............. ... .. .... ........ .. .......... .... ......... ... .................... ......................................................... .. ................... 55 66. Cross-bedded basal conglomeratic sandstone of the Altamaha Formation cuts underlying Tobacco
Road Sand ......... ... ........................ .. .. ..... ........... ... ........... ..... ... .... ... ... ... ........... .......................... .. ............ .... .... .. .. ...... 55 67. Ironstone and quartz pebble conglomeratic sandstone at same stratigraphic horizon as in Fig. 66 .......................... 56 68. Subtle, west-dipping contact between the semi-polygonal jointed sandstone of the Altamaha Formation
overlying the more massive Nanafalia Formation .............................................................,................................. ..... 56 69. Lag pavement of ironstone pebbles and cobbles overlying bleached Altamaha Formation sandstone ..................... 57 70. Basal chert clast conglomerate at Altamaha Formation- Tobacco Road Sand contact....... ... ..... .... ... ... .................. 57 71. Increasing downward mottling of Altamaha Formation sandstone......... .............. ........................ ............................ 58 72. Increasing downward mottling of Altamaha Formation sandstone............................................................ ............... 58 73. Mottled zone in Tobacco Road Sand cut by cross-bedded, basal conglomeratic sandstone of the
Altamaha Formation .................. .... ...... .............. ... ........................................ ....................... ............ ..... ............... .... 59 74. Unusual, high level, conglomeratic channel fill ................................................................................. ...................... 60 75 . Normal fault with bedding dipping in opposite directions ..................................................................... .. ................ 65 76. Faulted contact between brick-red sandstone of the Altamaha Formation and clay of the Tuscahoma
Formation ..... ........ .... ... .......................................... .. ................................................ ......................................... ........ 66 77. Faulted contact between kaolin and sandstone of the Nanafalia Formation ........ .. .............................................. .. ... 66 78. Deeply weathered fault within the Nanafalia Formation .......................................... ................................................ 67 79. Fault with Altamaha Formation on left and on top of Nanafalia Formation kaolin overlying Clayton
Formation clay and iron oxide residuum on right .. ......................................... ......... .. ...... ....... ........... ... ........ .. ......... 67 80. Faulted contact of the Claiborne Group sandstone overlying the Tuscahoma Formation clay.... ......... .. ... ....... .... .... 68 81 . Drag fold developed in sediments of the Tuscahoma Formation and overlying Claiborne Group
adjacent to a graben structure at the extreme left of the photo (dark red) .. ........ .. ..... .................. .. .. ....... ................ . 68 82. Graben structure shown at the extreme left in Fig.. 79 .. ..... .... .... .. ... .. ... ...... ..... ..... ........... ...... ......... ........ ........ .. ... ..... 69 83. Closeup view of the right side of the graben structure shown in Figs. 79 and 80 suggests a downward
bifurcation of this fault ...... ... .. .. ... ... .. ..... ..... ............. ....... ..... ...... ... .... ... ..... .... .. ......... ... .. ................. .... ... ... ... .. .. .......... 70
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84. NW striking fault developed in Altarnaha Formation and underlying softer Tobacco Road Sand........................... 71 85. Same structure viewed several years later after landfill pit has been partially filled ...................... ...... .................... 71 86. Multistage jointing with associated kaolinization and bleaching of the surrounding Nanafalia
Formation sandstone .............. .... ..... ... .. ....... ... ...... .. .. .. ........ ..... .. ........ ........... ..... ... ................ ... ... .................... ..... ..... 72 87. Large N-S trending joint or fault? (dark brown) cutting north dipping sandstone and kaolinitic
sandstone of the Nanafalia Formation ..................................................................................... ................................. 72 88. Joint cutting Providence Formation sandstone beneath unconformity with Nanafalia Formation
sandstone ...... ......................................................................................................................... ................................... 73 89. Iron oxide stained joint cutting older mottled sandstone of the Nanafalia Formation .... .................. .. .. .................... 73 90. Unusual vertical structure cutting Nanafalia Formation sandstone .... ............ .... ................... ............................... .... 74 91. Synclinal fold developed in Providence Formation sandstone ................................................................................. 75 92. Large anticlinal fold developed in Oligocene-age (?) Tobacco Road Sand and which is cut by fluvial
sandstone and channel sands of the Miocene-age Altamaha Formation........ .. ....................................................... .. 75 93. Map of Cenozoic faults in the Southeastern Coastal Plain and Piedmont.. .... ....................... .. ................................. 76 94. Kaolin and kaolinitic sandstone within sandstone of the Nanafalia Formation ........................................................ 78 95. Nanafalia Formation kaolin unconformably overlain by Altamaha Formation sandstone ........................................ 78 96. Erosion gully developed in soft Providence Formation sandstone .... ............... .......... ...... ........................................... 82 97 . Erosion gully developed in soft Providence Formation sandstone .. ........ .................................. ... ............................... 83 98. Erosional undercutting of soft Claiborne Group sandstone leads to collapse of box culvert and closure
of paved county road ......... .. ..................... .. ........ ....... .. .. ... ... .. ... ... ....... .. ... ... .. .. ..... ..... .. .......... .... .. .. .. .... .. ... ... ...... ........ 83 99. Erosion of soft Providence Formation sandstone leads to sedimentation and filling of storm culvert
under railroad tracks......... ..................................................... ... .... ............................................................................ 84 1OO.Erosion of soft Providence Formation sandstone leads to sedimentation and covering of railroad tracks ............... 85 101.Sedimentation results in shallowing and infilling of streams.................................................................................... 85 102.Shallowing and infilling of streams leads to degradation of habitat through increased water
temperatures, decrease in stream velocity, and drowning of vegetation................................................................... 86 103.Formation of stagnant ponded water and drowning of vegetation.................... ........................................ ................ 86 104.Deforestation of wetlands resulting from sedimentation ............... .... .... ........... .... ................. ................... ................ 87 105.Erosion gullies develop into illegal trash disposal sites that may contaminate the Claiborne aquifer................... ........ 87 106.Erosion gullies develop into illegal trash disposal sites that may contaminate the Claiborne aquifer......................... .. 88 107.Erosion gullies develop into illegal trash disposal sites that may contaminate the Claiborne aquifer .. ........ ...... .... ... .... 88
PLATES 1. Geologic map of the Eufaula South 7.5 minute quadrangle. 2. Geologic map of the Hatcher 7.5 minute quadrangle. 3. Geologic map of the Morris 7.5 minute quadrangle. 4. Geologic map of the Carnegie 7.5 minute quadrangle. 5. Geologic map of the Doverel 7.5 minute quadrangle. 6. Geologic cross-sections.
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INTRODUCTION
Scope of the mapping project
The Georgia Geologic Mapping Program mapped the surface geology of the Carnegie, Doverel, Eufaula South, Morris and Hatcher 7.5 minute (1:24,000 scale) quadrangles in the Upper Coastal Plain of southwestern Georgia from October, 2006 through June, 2007. Mapping included both traditional field mapping and development of GIS digital databases for each quadrangle in Arclnfo format. Mapping was part of the Georgia Geologic Mapping Program's STATEMAP Project (in cooperation with the United States Geological Survey, Cooperative Agreement #06HQAG0044).
The Georgia Geologic Mapping Program's STATEMAP Project involves the geologic mapping of significant aquifer recharge zones in the Upper Coastal Plain (Fig. 1). These recharge zones include those of the Cretaceous, Clayton, Claiborne, and Upper Floridan aquifers. Previously funded STATEMAP mapping in Georgia (Fig. 2) included 18 quadrangles of the Americus area and compilation of that mapping as a 1:100,000 scale geologic atlas of the Americus area. In the Lumpkin project area, three quadrangles were mapped for 2004, four quadrangles for 2005, and four quadrangles for 2006. Figure 3 provides a summary of the stratigraphy and related aquifers in or adjacent to the Lumpkin project area.
Methods
Field methods used to produce the geologic maps (Plates 1 through 5) involved mainly the description and mapping of roadside outcrops and exposures. In addition to the geologic mapping, lithologic descriptions of well cuttings from the Georgia Geologic Survey technical files and published descriptions from Herrick (1961) were used to help construct the geologic cross-sections illustrated in Plate 6. The Georgia Geologic Mapping Program drilled a series of shallow core holes (less than or equal to 50 feet) that were designed to: 1) confirm the mapped geology, 2) determine depth to contacts, and 3) examine relatively non-weathered lithologies particularly in areas with limited exposures.
A significant part of this project involved production of digital mapping products. Outcrop locations were digitally plotted directly from field maps using Arclnfo 9.1. Additional field geologic data were compiled in an Arclnfo database. Digital geologic maps were compiled on-screen using the outcrop data and cross-sections (Plate 6). Arcplot programs were written to prepare hard copies of each individual geologic map (Plates 1 - 5). Geologic cross-sections were constructed on gridded mylar, scanned, digitally traced and graphically completed in CorelDraw 7.0. Documentation regarding the development of the Arcinfo databases as well as Arcinfo export files of those coverages are in preparation. Development of the Arclnfo databases for the current map area generally follows the procedures documented for the previous STATEMAP quadrangles in Georgia (Cocker, 1999b, c, d and 2000a, b, c, d).
Lithologic descriptions and stratigraphic terminology (Fig. 4) for this portion of the Lumpkin STATEMAP Project generally follow that of Cocker (2003b; 2004), Eargle (1955), Hetrick (1990), Marsalis and Friddell (1975), and Reinhardt and others (1994).
1

Figure 1. Location of the Lumpkin project area in relation to the most significant groundwater recharge areas. The most significant groundwater recharge areas are shaded.
2

EXPLANATION

Map coverage @ 1: 100,000 scale



Wrens-Augusta (GGS, Hetrick, 1992) Kaolin District (GGS, Hetrick and Friddell, 1990) Fort Valley (GGS, Hetrick, 1990)

Butler (GGS, Hetrick, 1996)

:- ~ Americus 30' x 60' (USGS, Reinhardt and others, 1994)
Map coverage @ 1:24,000 scale
0 Americus Project- STATEMAP (completed 2003)

Lumpkin Project- STATEMAP (in progress)

N

Seal~
(approximuLc)

0

SO miles

Figure 2. Map of Georgia showing location of STATEMAP mapping and previous 1:100,000-scale Upper Coastal Plain geologic mapping.

3

Period Quaternary

Epoch Recent
Pleistocene
Miocene

Eocene to Oligocene

Fonnation unnamed stream alluvium mmamed sf ream alluvium
Allatnalta Fonnatiolt
Residuum from Eocene and Oligocene limestones. M1y include units as old as the Lisbon FonnatiOJt

Group Vicksburg Group

Aquifer

Tertiary

Eocere

Ocmulgee Formation Williston F01mation Muckalee Formation
Clinchfield Formation
Perry Sand/Lisbon Formation Tallabaua Fonnation
Hntcheligbee Formation

Ocala Group

Upper
Floridan Aquifer

Barnwell Group Claiborne Group

Claiborne Aquifer

Tuscahoma Formation

Wilcox Group

Paleocere

Nanafidia Fonnatiou
Porters Creek Formation Clayton Fonnation

Midway Group

Clayton A<tuifcr

Providence Formation

Providence Aquifer

Cretaceous

Gulftan

Ripley Fonnation Cusseta Sand Blufftown Fonuation
Eutaw Formmion

Selma Group Eutaw Group

Cusseta Aquilbr
EutawBJuCftown
Aquifer

Tuscaloosa Formation

Tuscaloosa Grout>

Comanchean

Undi fferentiatcd

Ftg. 3. Stratigraphy and related aqutfers m or adJacent to the current map area. (* Upper part of Tuscahoma Formation may be Lower Eocene in age). Units in italics are absent or not recognized as distinct, mappable units.

4

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Map Unit Symbol

Unit De!!cription

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Ta

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Tsr

~

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cu<>:
~

:a..2

Tcb

-~ ~
~~ ~

-j~

Ttu

g

" g

'* J'.!.I Tnf

"u""
0.

'II

0.

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j.""

Tpc

"~ "'
~:1:~: "~'

Tel

:::E

~

Kp

a!

u'2

Kr

t

:3=

Kc

Quaternal'y alluvium variably mi~ae<:OlLS nnd clayey, poorly-sorted, sill, sand, and qunrtz gravel.
\lt:mulhn Fotmlllilm - cllm1innntly mw; 'ivc, hri.-!H ~d . nrgillnc~ous sn nd<;tonc nnd mottled clll)'-ridl sandstone~ '' ith pea to .;<1bbl.: (nm:}- siLo:! iron shlll ~ .:I MH~, unuomnwn 'lnm1z p bhl~ h~1ls. ~nd rnN ch~rt ch~r.<:. Conglomerat ic lny.:r commonly l~nnut ul. lo wcr ,unln cl \\'~h ' luibome in111p snnds cont~ itL~ irJOSfone clasl~ nnd IJllln1Z p.:bldc. . und locnlly iron O!-.id.: ..:nil;!~ nnd rottnd~d. c bhle to h o uhl.:r-~ iz~:d c hl ~t.. o!' ~n ndslott c apparently d.: rivild from cmsicm of' tut d~rlyint,: Ct:tibomc Group s.:dimcnts. Te.rfiiH'y Sl'lllnumts and Residuum - variably waxy to slightly silty clays that commonly include abundant chert .
Removed by erosion or not r~cognized; mny be part of the Tutial)' S~dim~nts and Residuum.
OnlhonJcGroup: l'eiTJ' Sand lim:- to 1!0: . ~-er~tn.:d, masshe- fll crnss-b<lrld~d ~~nd gmding downdip to l.i;bon l\mnnlion. Lisbon Fo.nnofton tn(,';lron s. s:Uldy d ;ty, d :ty.:y snnd, nnd l im~-sione TuiJnhntta Fmm:&llon - mn~s-iv.:-- 1~1 ern <> -hedd~,~ lin~ to t:<lll r,'$c-gr.1itlod, li ncl)' layered to cros~ bcddcd sand and snndstou.: uti rlay~rcd wiih 11\'(1 1ltln shales to sandy sha l o~. l'crry 'and mny h C<tLJi\'IIICnt io Ta llahnlta F,)mlati<m. 1'uscahomo l1nm1atlon - nonfossiliJ'i:rotL~. carbonaL'C<lUS, clay, silt, and sand overlying and latornlly grading into cross-bedded.micac.:ous. ,,a(I!IWou~. fossiliferous, medium- to coan.~-grained sand.
NunafuBa I<'onruttion- micaceous, m~s.siv.:-bcddcd, glauconitic, fossiliferous, calcareous, tin~- to conrne-grain~d sand with local clny lenses.
,
Porters Creek Fonnation- tiJs.~iltfcr.JtLS, glauconitic. flll~ilc, waxy to Yariably silly cia):
C'lllytml Fcmnntton - S<UJdy, rnicritic, bioclastic limestone with itltcr-bedd~d silty clay and c:tkareou~ samMo11C.
Providence Fonn11tlon- kuolinitic. croSJ:-!Jedded, mediwll coars~>gnlirted sund und SIUtdstonc with locnl koolin
lens~s
Ripley Fom1atlon- mas~i\c. micaceous and glanconitic. fine- gruined saud nod silly clny
Cusseta Fonuatlon cross-bedd.!d. locally kaolinitic, medium to conrsc-t,'l'ained snnd

Kb

Bluffiown I<ormntlon- glauconitic. calcarl!ous, fin.: sand owrlain by carbonaceol~~ clay 1111ti silt, cross-bedd.-d

snnd..and hi.,hlv fhssilif,rorc~ dav to 1>lauconitlc fine sand

Figure 4. Summary descriptions of the map units in the current map area.

Previous investigations

Recent regional scale maps (1:100,000) are located in relation to the STATEMAP quadrangles in Fig. 2. The quadrangles mapped during this current project are adjacent to the Georgetown, Sanford, Cuthbert, Martins Crossroads and Shellman 7.5' quadrangles (Cocker, 2001, 2004a, 2005b, 2006).

5

The Geologic Map of Georgia (Georgia Geologic Survey, 1976) and the 1:500,000 scale Digital Geologic Map of Georgia (Cocker, 1999) provide a general view of the surface geology of the map area. Digital overlays of the geology and topography @1:24,000 scale display a rough correlation between the 1:500,000 scale geology of the state map and the detailed topography.
Other geologic investigations in or near the present map area are concentrated mainly on the stratigraphic sections exposed along the Chattahoochee River that were exposed prior to flooding of the Walter F. George Reservoir. Geologic reports that provide pertinent information or aid in interpretation to the present mapping include local and regional studies by Beck (1982), Bybell and Gibson (1982), Cocker (2001, 2002, 2003a, b, 2004a, b, 2005a, b), Cocker and Costello (2003), Cramer and Arden (1980), Eargle (1955), Fallaw and Price (1992), Fritz (1989), Gibson (1982), Gohn and others (1982), Herrick and Vorhis (1963), Hetrick (1990, 1992, 1996), Hetrick and Friddell (1990), Huddlestun (1985, 1988, 1992a, b, 1993), Huddlestun and Hetrick (1979, 1985, 1991), Huddlestun and others (1974), Kirkpatrick (1959, 1963), Marsalis and Friddell (1975), Nystrom and Willoughby (1982), Owen (1956), Reinhardt (1982, 1986), Reinhardt and Gibson (1981), Toulmin and LaMoreaux (1963), Toulmin and others (1964), and Zapp and Clark (1965).
Few deep drill holes are available for the present map area. Subsurface geologic investigations of the study area include descriptions of well logs and hydrologic reports. Lithologic descriptions of core samples and cuttings from wells in Quitman and Randolph Counties were obtained from published data by Herrick (1961), and unpublished drill logs by Herrick and anonymous authors (Georgia Geologic Survey technical files, Atlanta, Georgia). Many core logs and stratigraphic determinations (if present) are not of sufficient quality and consistency for constructing accurate cross-sections. Clarke and others (1983, 1984), Gorday and others (1997), Johnston and Miller (1988), Long (1989), McFadden and Perriello (1983), Mitchell (1981), Reinhardt (1982), and Vorhis (1972) examined the hydrology and hydrogeology of the region.
Soil characteristics vary considerably over the mapped area. Those soils derived from poorly cemented sands and silts such as the Tallahatta Formation of the Claiborne Group and the Providence sand are prone to rapid erosion. Clay- or silt-rich stratigraphic units, e.g. the Tertiary sediments and residuum unit, clay residuum of the Clayton Formation, the Tuscahoma Formation and the Ripley Formation, yielded poor clayey soils. The Altamaha Formation is a mixed sand and clay unit overlying much of the eastern part of the map area, and yields a rich loam type of soil.
PHYSIOGRAPHY AND LAND USE
The Carnegie, Doverel, Eufaula South, Morris and Hatcher quadrangles lie within the Coastal Plain Physiographic Province. Terrain in the Carnegie and Doverel quadrangles differ significantly from that Eufaula South, Morris and Hatcher quadrangles further to the west.
Terrain in the Doverel quadrangle is relatively flat with relief between the broad interfluves and the stream valleys on the order of about 80 feet. Topography is influenced mainly by the Ichawaynochaway Creek and its tributaries, Walk-Ikey Creek, Falling Creek, and Pruitt Creek as they have cut down through the more resistant Altamaha Formation into the softer Claiborne Group sandstone. Stream valley bottoms are wide- on the order of 2000 to 3500 feet in the Ichawaynochaway Creek valley. Drainage appears relatively poor in the interfluves with few secondary streams and numerous marshes and ponds on the topographic map. The upland areas slope gently
6

from 390 feet near Shellman in the northwest to 280 in the southeast. The Carnegie quadrangle lies astride the divide between the Flint and Chattahoochee River basins. Carter Creek
and its tributaries eventually join up downstream with Ichawaynochaway Creek and drain into the Flint River. Cemochochechobee Creek and Hog Creek flow westward eventually into the Chattahoochee River. Relief between the interfluve areas and the stream bottoms are on the order of 90 to 120 feet. Interfluve areas are narrower and generally gently sloping. Stream valleys are generally narrow with only Carter Creek having about a 1000 foot wide valley bottom. The upland areas slope gently from 490 feet in the northwest to about 380 in the southeast. Streams have cut down through the more resistant Altarnaha Formation into the softer Claiborne Group sandstone.
West and north of Cuthbert in the Morris and Hatcher quadrangles, physiography is dominated by Pataula Creek and its tributaries, especially Holanna and Hodchodke Creeks. In the western part of the Hatcher quadrangle the South Fork of Tobanee Creek, Drag Nasty, and smaller unnamed creeks empty into the Chattahoochee River. Except for the southwestern comer of the Hatcher quadrangle, most of the terrain is hilly. Relief is generally on the order of 150 feet between the top of interfluves and the adjacent creek bottoms. Valley bottoms of the larger creeks, Pataula, Holanna and Hodc~odkee Creeks, are generally flat and wide about 2000 feet. The others are generally rather narrow. Creeks have cut down through the relatively soft Nanafalia and Providence Formation sandstones. Relatively wide flat interfluve areas in the southwestern comer of the Hatcher quadrangle are underlain by the Providence Formation. Base level of the Chattahoochee River flood plain is on the order of 195 to 200 feet, because of the Walter F. George Reservoir. The hilly terrain is characteristic of the Fall Line Hills physiographic district. An escarpment that extends through the southeastern part of the Morris quadrangle reflects breaching of the Altamaha Formation caprock and rapid down cutting through the Claiborne Group and Tuscahoma Formation.
In general, flat bottomland in the major stream valleys is commonly sandy and marshy, and is ill-suited for either development or agriculture. The wider interfluve areas in the Doverel, Carnegie and Hatcher quadrangles are generally suited to agricultural development. Agricultural products may include pasture, cotton, pecans, beef cattle, sawlogs and pulpwood.
The major population centers of Cuthbert, Ft. Gaines, and Georgetown are outside of the current map area. Abundant, retirement and vacation housing has been built near the Walter F. George Reservoir. These structures and numerous roads are not reflected on the rather dated topo~aphic maps (1967- 1968 vintage).
SOILS
In the Georgetown quadrangle, flat land best suited for agriculture is present along the Chattahoochee River. Soils along the Chattahoochee River are derived mainly from the Cusseta Formation and various alluvial materials. Much of the remaining area is underlain by poor, generally sandy soils derived from the Cretaceous age sedimentary units.
In the eastern part of the Cuthbert quadrangle and over much of the Brooksville and Martins Crossroads quadrangles, broad expanses of relatively flat land are utilized for pecan orchards, farming, and cattle. These broad expanses are mainly underlain by the Altamaha Formation with smaller areas underlain by the Tertiary sediments and residuum unit and the Claiborne Group. The argillaceous sandstone of the Altamaha Formation provides the best soils suited to agriculture. Areas underlain by clays of the Tertiary sediments and residuum unit and sands of the Claiborne Group are best suited for orchards, pasture and forest products.
7

Soils in the map area reflect intensive subtropical weathering of the exposed Tertiary and Cretaceous stratigraphy. Soils may be classified based on diagnostic surface horizons, epipedons, and subsurface horizons. The principal types of soil found in the southeastern United States are Ultisols. This soil order is characterized by argillic or kandic horizons and low base saturation. An argillic horizon is defmed as a subsurface accwnulation of high-activity silicate clays that have moved downward or translocated from the upper horizons or have formed in place (Brady and Weil, 1999). An epipedon overlying a kandic horizon has commonly lost most of its clay content. A kandic horizon is a diagnostic subsurface horizon characterized by an accwnulation of iron and aluminwn oxides as well as low activity, strongly acid, silicate clays (e.g., kaolinite). Low activity clays demonstrate low cationholding capacities (< 16 cmolcfkg clay). Clays are often found as coatings on pore walls and surfaces effectively reducing porosity and permeability. Precipitation of thin coatings of iron oxides on these clays and quartz sand grains effectively gives many of the sandstone units a reddish color. More reducing conditions result in more browns and less reds in the soils and or rock units. Mobilization and precipitation of clays and iron oxides has the effect of obliterating primary sedimentary textures such as cross-bedding. Ultisols formed under conditions of fluctuating wetness have horizons of iro~-rich mottled material called plinthite. As long as it remains moist, plinthite is soft and easily dug. When exposed and dried in air, plinthite hardens into an ironstone. Ultisols are formed under wet, tropical conditions and usually under forests. Most are developed on old land surfaces (Brady and Weil, 1999).
Intensive subtropical weathering has produced a commonly striking profile in the soils and subsoils, particularly in those derived from the Altamaha Formation. The upper portion of the profile is commonly sand-rich or slightly argillaceous sand/sandstone. This portion of the profile may range from 0 to 5-10 feet thick. Thickness of this sandy portion of the profile is commonly dependent on the degree of erosion (Long and Baldwin, 1915). A clay rich zone is generally found beneath the upper sandy zone or may be present by itself with the upper, sandy unit having been removed by recent erosion. Clay particles are mobilized by downward percolating surface water and accumulate in the subsoil. Mottling, probably related to oxidizing ground water, is usually developed in the clay rich lower zone. Irregular concentrations of iron-oxide cemented sediments (plinthite) may be developed in this lower clay-rich zone. These have formed in situ and result from remobilization of iron from other parts of the soil and subsoil. Cocker (200 1) described and interpreted the vertical distribution of particle sizes in the main soil types of the Bottsford, Dawson, Parrott and Shellman quadrangles just to the east of the current map area. These relationships should generally exist in the Cuthbert, Brooksville and Martins Crossroads quadrangles where the Altamaha Formation is located.
GENERAL GEOLOGY
The surface geology of these five quadrangles is quite varied, with mainly Eocene and younger Tertiary sediments exposed over most of the Carnegie and Doverel quadrangles. Upper Cretaceous and Paleocene sediments are dominant in the Eufaula South, Hatcher and Morris quadrangles. Portions of the Morris quadrangle contain the Altamaha Formation and Eocene sediments. Younger sedimentary rocks are dominant in the eastern quadrangles because of the regional southeasterly dip. Erosional unconformities, facies changes, surface weathering, groundwater alteration, lithologic similarities of some sedimentary units, and paucity of outcrops, as well as various combinations of these factors add complexities to the identification and mapping of the rocks in the Morris and
8

Hatcher quadrangles. As in the area covered by the Americus geologic atlas (Cocker, 2003b), the youngest Tertiary sediments,
represented by predominantly argillaceous sandstone of the Miocene Altamaha Formation, formerly covered most if not all of the present map area. Erosional remnants of the residuwn of Eocene and Oligocene age sediments, represented mainly by clay and chert, are found in the Carnegie and Doverel quadrangles. Generally soft, unconsolidated or poorly cemented sandstone of the Middle Eocene Claiborne Group is found on slopes and on locally large portions of the upland areas in the Morris, Carnegie and Doverel quadrangles. The Upper Paleocene Tuscahoma Formation is found on the erosional escarpment in the southern part of the Morris quadrangle. Apparent local and probably regional variations in thickness are evident in the Tuscahoma Formation and Claiborne Group. Kaolinitic, micaceous, cross-bedded sandstone of the Upper Paleocene Nanafalia Formation is found to crop out in the Morris and Hatcher quadrangles. A few, scattered occurrences of a clay and iron oxide residuwn of the Lower Paleocene Clayton Formation are found in the Hatcher and Morris quadrangles. Upper Cretaceous Providence Formation sediments are exposed in the Eufaula South, Hatcher and Morris quadrangles. Clay, silt and marl of the Ripley Formation are found along the shores of the Walter F. George Reservoir. Subsurface information regarding the Upper Cretaceous stratigraphic section is sketchy within the present map area and thicknesses of these units are poorly known in this area.
Regional dip of the Upper Cretaceous and Tertiary sediments older than the Altamaha Formation is on the order of 10 to 30 feet per mile to the southeast. Locally, sediments and contacts dip to the north and may reflect reversal of dips caused by folding. Folds are particularly evident in the southern part of the Morris quadrangle. Although the lower contact of the Altamaha Formation is locally very irregular because of an erosional disconforrnity with underlying sediments, it dips generally gently to the southeast, also. Total thickness of the Upper Cretaceous section is unknown, because of the lack of deep and detailed drill hole data. The Tertiary section increases in thickness from the west and north to the south and east. Maximwn thickness of the Tertiary section in the southeastern part of the map area is on the order of 400 - 500 feet.
Accuracy of well locations is highly variable. Most of these wells were drilled for water supply purposes, and some were apparently not surveyed. Prior to the 1970s, 7.5-minute quadrangle maps were not yet available for this part of Georgia, and well locations were marked on Georgia Department of Transportation county road maps. Well locations were subsequently transferred to other maps in the Georgia Geologic Survey technical files. One GIS database was developed from wells plotted on Georgia Department of Transportation (DOT) county road maps that are located in the Georgia Geologic Survey technical files . Well locations were then plotted on digital images of each DOT county road map, and attributes were added in ArcView.
Another GIS database was developed from an earlier, unpublished digital database of GGS nwnbered wells that were located by latitude and longitude. A digital plot of both of those databases together show some of the same wells from each database to lie close to each other while others are either missing from one of the databases or they are relatively far apart. A comparison with data on the well log sheets as well as the probable location for a well on a topographic base map, suggests that the database that contained latitude and longitude data for the GGS wells is generally the more accurate database. Actual locations of these older wells still could be several hundred feet from the positions plotted on the accompanying geologic maps, as the precision of the latitude and longitude data does not allow a more accurate plot.
9

Locations of wells from the DOT maps were used when those wells were not included in the GGS digital database. Locations of all the wells in the current map area are shown on Plates 1 through 5.
STRATIGRAPHY OF THE CARNEGIE, DOVEREL, EUFAULA SOUTH, MORRIS, AND HATCHER QUADRANGLES
Exposed stratigraphic units in the study area include the Upper Cretaceous Ripley (Kr) and Providence (Kp) Formations, Paleocene Clayton (Tel) and Nanafalia (Tnf) Formations, Upper Paleocene Tuscahoma Formation {Ttu), Middle Eocene Claiborne Group (Tcb), the Miocene Altamaha Formation (Ta), Tertiary~Quaternary Alluvium (TQal), and Quaternary Alluvium (Qal). An additional map unit, the Tertiary Sediments and Residuum unit (Tsr), is believed to consist of unidentified portions of Eocene and Oligocene stratigraphic units and their residuum. Descriptions ofthese units are summarized in Figure 4.
Upper Cretaceous Exposed Upper Cretaceous sediments in the map area include the Providence and Ripley Formations. Recent
studies of the Upper Cretaceous sediments from eastern Alabama to the Flint River indicate that most of the Upper Cretaceous units contain two or more lithofacies (Rheinhardt and Gibson, 1981). These include a continental facies and a marine facies. Generally, the basal and downdip portions of these units are representative of the marine facies.
In addition, asymmetrical depositional cycles composed of regressive and transgressive phases are developed in the Upper Cretaceous sediments (Rheinhardt and Gibson, 1981). The regressive phases representing progradation are thicker and better developed. Progradation may be due to sedimentation rates greater than basin subsidence or to a gradual drop in sea level. Descriptions of the lithologies and their depositional environments are discussed in Rheinhardt and Gibson (1981).
Selma Group Ripley Formation (Kr)
The lower part of the Ripley Formation consists of a massive, bioturbated, fme to medium grained, micaceous, glauconitic, calcareous quartz sand. The upper part of this unit is commonly massive, fme sand to silty clay. Near the top of the Ripley Formation, grain size increases abruptly, may contain a bone and shell lag, and is well bedded. Thickness of the Ripley Formation ranges from 135 feet up dip to 250 feet downdip (Reinhardt and others, 1994). Generally, the Ripley Formation is a relatively fossiliferous unit. Older sediments of the Ripley Formation were deposited in an inner shelf environment. Younger sediments were deposited in a barrier island complex. The top of the Ripley Formation was marked by abrupt shallowing and subaerial exposure with development of paleosols (Rheinhardt and others, 1994). The Ripley Formation is exposed only along the Walter F. George Reservoir (Fig. 5). Lack of a boat and operator prevented a careful inspection ofmore of these exposures.
10

Figure 5. Exposure of Ripley Formation on shore of Walter F. George Reservoir. Eufaula South quadrangle.
Providence Formation (Kp)
The Providence Formation is the youngest Upper Cretaceous unit in the cmrent map area. Reinhardt and others (1994) describe the Providence Formation as pale yellow, cross-bedded, locally micaceous, fine to coarse sand with inter-bedded, yellowish brown to olive, massive to thinly"bedded, sandy clay lenses. This unit is subdivided in crosssections into two lithofacies. The up dip lithofacies consists of cross-bedded, coarse quartz sand with locally abundant heavy minerals. The heavy mineral suite consists mainly of ilmenite, zircon and rutile and locally may constitute up to one third of the sand (Rheinhardt and Gibson, 1981). The down dip lithofacies is a laminated to massive, highly micaceous, locally carbonaceous, silty clay and clayey fme sandstone. Both lithofacies may be butTowed or biotmbated. The up dip lithofacies was divided into an upper and lower cross-bedded sand by a 20 inch thick sandy clay bed (Donovan, 1985). Thickness of the Providence Formation may range from 83 to 267 feet (Marsalis and Friddell, 1975; Reinhardt and others, 1994). Kirkpatrick (1959) described the Providence Fonnation as being 140 to 160 feet thick.
Outcrops of the Providence Formation in the Hatcher quadrangle display a pronounced increase in grain size, with locally abundant large rounded quartz and quartzite clasts (Figs. 6 - 13). The basal Perote Member is 10 to 35 feet thick and consists of thinly bedded, dark-grey, highly micaceous and lignitic, sandy silt and clay. This grades
11

upward to fine sand and eventually to medium to coarse, cross-bedded sands of the upper member. Donovan (1985) and Reinhardt and others (1994) consider the Perote Member to be the upper part of the Ripley Formation. Marsalis and Friddell (1975) described the Perote Member as the basal part of the Providence Formation. The upper member of the Providence Fonnation consists of variegated white to yellow to orange, micaceous, feldspathic, cross-bedded, medium- to very coarse-grained sand (Marsalis and Friddell, 1975).
Induration of the Providence Fonnation varies considerably from relatively hard sandstone, to soft sandstone, to soft sand/sandstone. Headward erosion into the generally soft sand and sandstone of the Providence Formation has cut steep, cliff-like scarps. Most of this erosion is related to rapid downcutting by streams in the Chattahoochee River Basin (Cocker, 2005).
Trace fossils consisting of clay-lined, Ophiomorpha burrows are locally abundant in cross-bedded sandstone (Rheinhardt and Gibson, 1981) and are classified mainly as belonging to the Skolithos ichnofacies (Frey and Pemberton, 1984). These Skolithos ichnofacies are indicative of relatively high levels of wave or current energy, typically developed in clean, well-sorted, loose or shifting particulate substrates (Frey and Pemberton, 1984). The occurrence of this ichnofaci~s with large and small-scale trough cross-bedding indicates a near-shore environment such as on the foreshore and shoreface of beaches, bars and spits (Frey and Pemberton, 1984). These burrows are usually developed in soft sand and do not weather well.
Figure 6. Cross-bedded, gravel-rich sandstone and conglomerate of the Providence Formation. Northwest comer of the Hatcher quadrangle.
12

Figure 7. Gravel-rich sandstone ancl conglomerate of the Providence Formation. Borrow pit in southwest corner of the Hatcher quadrangle.
Figure 8. Coarse gravel-rich conglomerate unconformably cutting sandstone of the Providence Formation. Central part of the Hatcher quadrangle .
13

L

o

Figure 10. Interbedded coarse gravel-rich conglomerate and sandstone of the Providence Formation. Central part of

the Hatcher quadrangle.

14

Figure 11. Gravel-rich conglomerate of the Providence Formation. Southeast comer of the Hatcher quadrangle. 15

Figure 12. Thick, coarse gravel-rich conglomerate Formation. Central part of the Hatcher quadrangle.
16

Providence

Figure 13. Outcrop of Providence Formation sandstone with the eastern (right) portion stained red by iron oxide. Note that iron oxide staining is not related to present topography. Hatcher quadrangle.
Lower Paleocene Midway Group Clayton Formation (Tel) The Clayton Formation is described as being composed of yellow to buff-brown, interbedded, micaeous silty.
clay, calcareous sandstone, and bioclastic limestone (Reinhardt and others, 1994). The limestone is described as locally well-crystallized and well-cemented or vuggy and is composed of molluscan and bryozoan fragments. In the Chattahoochee River area, the Clayton Formation is described as: 1) a basal conglomerate overlain by interbedded grayish-yellow sandy, shelly limestone and calcareous sands; 2) a white to gray, dense limestone with oyster shells and other fossil debris; and 3) an upper white to gray microfossiliferous, massive limestone (Cramer and Arden, 1980; Marsalis and Friddell, 1975; Toulmin and LaMoreaux, 1963). At Ft. Gaines, exposures along the Chattahoochee River (Figs. 14 - 17) are of rhodolithic or foraminifera-bearing limestones (Figs. 15, 16). Here, the upper surface of the Clayton Formation is a deeply eroded paleokarst surface (Fig. 17) that has been overlain by transgressive, channel-fill sands of the Gravel Creek Member of the Nanafalia Formation (Bryan, 1993).
The few, limited exposures (Fig. 18 - 24) of the Clayton Formation in the present map area consist of a residuum of red, buff to dark brown, white to light gray and black clay with layers and irregular masses of iron oxide. Occasionally, a few exposures contain chert. The northernmost exposure of Clayton Formation limestone on the Chattahoochee River is at river mile 81 (Toulmin and others, 1964) which is located about 4.5 miles south of the Hatcher quadrangle. The transition from no limestone in the Hatcher quadrangle to limestone in the Ft. Gaines quadrangle is rather abrupt. Similar relations were documented in the County Line quadrangle where exposures of Clayton Formation limestone change rapidly to clay and iron oxide residuum over an interval of less than 2000 feet
17

(Cocker, 2005b). Intensive physical weathering of Clayton Formation clay, as well as extensive paleo-erosion at the base of the Nanafalia Formation and more recent erosion apparently has removed most of the Clayton Formation in the Hatcher and Morris quadrangles. Regionally, thickness of the Clayton Formation may range from 10 to 165 feet (Marsalis and Friddell, 1975; Owen, 1956; Reinhardt and others, 1994). Cross-sections by Rheinhardt and others (1994) show regional thinning of the Clayton Formation, but the rapid lateral transition from isolated residuum remnants to apparently tmweathered limestone suggests a rather more complex situation.
Origin of the Clayton Formation residuum has received no recent attention. Iron oxide clasts from this residuum are found in the overlying fluvial sandstone of the Nanafalia Formation and Altamaha Formation indicating that development of this residuum is older than the Nanafalia Formation. The presence of basal Nanafalia Formation sediments in paleo-sinkholes (Fig. 17) as well as chert clasts containing Clayton-age fossils in gravel beds that are believed to be basal Nanafalia Formation also suggest a pre-Nanafalia age to the residuum. Replacement of fossil shells by iron oxides suggest reduced groundwater containing ferric iron encountered more oxidizing conditions, dissolved the carbonate and deposited ferrous iron oxides. Iron oxide geodes are commonly found in this residuum and indicate that some of the iron oxide deposition occurred in open voids, i.e. solution cavities(?).
Figure 14. Exposure ofkarstified limestone of the ClaytonFommtion immediately south of the Walter F. George Dam on the Chattahoochee River.
18

Figure 15. Rhodolithic limestone of the Clayton Formation immediately south of the Walter F. George Dam at Franklin Landing, AL on the Chattahoochee River.
Figure 16. Soft, benthic foraminifera bearing limestone of the Clayton Formation immediately south of the Walter F. George Dam at Franklin .Landing, AL on the Chattahoochee River.
19

Figure 17. Paleokarst "solution hole" filled with Gravel Creek Member sandstone of the Nanafalia Formation at Franklin Landing, AL on the Chattahoochee River.
20

Figure 18. Chert residuum of the Clayton Formation. Hatcher quadrangle.
Figure 19. Large chert boulder containing Clayton Formation fossils. Southern part of the Hatcher quadrangle. 21

Figure 20. Nanafalia Formation sandstone overlying soft Clayton Formation clay with soft sandstone and kaolin of the Providence Formation in lower part of gully. Morris quadrangle.
22

Figure 21. Iron oxide and clay residuum of the Clayton Formation. Northwest quarter of the Hatcher quadrangle.

Figure 22. Iron oxide pseudomorphs after calacareous fossils indicate replacement limestone rather than a near-surface ferricrete-type deposit. Hatcher quadrangle.

Clayton Formation

23

Figure 23. Small rerrmant of residuum of iron oxide and clay of the Clayton Formation between Nanafalia Formation sandstone on the right and Providence Formation sandstone on the left. Northeast comer of the Hatcher quadrangle.
Figure 24. Iron oxide and clay residuum of the Clayton Formation overlying Providence Formation sandstone on the right and underlying Nanafalia Formation sandstone on the left. Northwest comer of the Morris quadrangle.
24

Porters Creek Formation (Tpc)
The Porters Creek Formation may be is locally present as an oliv.e-black, compact, highly glauconitic, fissile clay to silty clay in western Georgia (Reinhardt and others, 1994). Thickness of this unit, where present, is 3 to 33 feet. Clays present in this stratigraphic position are considered to be clay and residuum of the Clayton Formation and is included as part of the Clayton Formation.
Upper Paleocene to Lower Eocene Wilcox Group Nanafalia Formation (Tnj)
In the current map area, the Upper Paleocene Nanafalia Formation is exposed in the Hatcher and Morris quadrangles. The Nanafalia Formation consists of cross-bedded, fme to very coarse, light greenishgray to yellowish-brown to white, highly micaceous quartz sandstone, kaolin and bauxite (Figs. 25-31). Black, heavy mineral sands are locally concentrated in the road drainage ditches. The sandstone may contain abundant, rounded or subrounded kaolin or bauxite clasts (Fig, 31). A conglomerate containing rounded quartz pebbles and angular chert clasts (Fig. 25) in the Hatcher quadrangle is a unique lithology not described elsewhere. It is believed to be a basal conglomerate of the Nanafalia Formation as it contains angular chert clasts of Clayton age residuum.
Because of poor exposure, the Nanafalia- Clayton Formation contact and the Nanafalia- Tuscahoma Formation contact were seldom observed in the current map area. Significant erosion since deposition of the Nanafalia Formation has removed or cut deeply into the Nanafalia Formation in a number of exposures.
The Nanafalia Formation is divided into two coeval lithofacies, the Baker Hill and Nanafalia Formations (Reinhardt and others, 1994). The Baker Hill Formation is described as consisting of fme to coarse, light greenish-gray to yellowish-brown, highly micaceous quartz sand that interfmgers with light greenish-gray to black sandy clay and massive kaolin beds. Trough cross-bedding and abundant rounded to subangular clay clasts are commonly found in the sandy intervals. Commonly thick-bedded to massive clay is locally more than 33 feet thick and may contain sand or silt laminae. The Gravel Creek Member, the marginally marine to nonmarine facies of the Nanafalia Formation (Huddlestun and others, 1974), is similar to the Baker Hill Formation of Reinhardt and others (1994).
According to Reinhardt and others (1994), the Nanafalia Formation is present only in the subsurface. This unit contains greenish-gray, micaceous, fme- to coarse-grained, glauconitic, fossiliferous, massive bedded, fossiliferous quartz sand with local clay lenses. Reinhardt and others (1994) note that the Nanafalia Formation may be 20 to 160 feet thick. Large, economic deposits of kaolin and bauxite are found in the Nanafalia Formation in the Andersonville, Springvale and Eufaula districts.
25

Figure 25.

angular clasts of

Fonnation chert and rounded quartz pebbles.

Basal. conglomerate of the Nanafalia Fonnation (?). Southern part of the Hatcher quadrangle.

26

Figure 26. Contact between overlying Nanafalia Formation sandstone and Clayton Formation clay and iron oxide fragments. Morris quadrangle.
27

Figure 27. Cross-bedded, kaolinitic, micaceous, cmlrs1~-gJrau1ea Nwnerous joints and faults cut this outcrop. Morris quadrangle.
.. ~
j 4:- .. ..,
Figure 28. Soft, kaolinitic, micaceous fme- to coarse-grained sandstone of the Nanafalia Formation. Morris quadrangle.
28

Figure 30. Kaolin lens or bed exposed in road drainage ditch in the Nanafalia Formation. Morris quadrangle.
29

Figure 31. Kaolin clasts in upper sandstone of the Nanafalia Fonnation. Morris quadrangle. Tuscahoma Formation (Ttu)
The Upper Paleocene Tuscahoma Fonnation (Figs. 32-33) is exposed mainly in the southern end of the Morris quadrangle. The Tuscahoma Fonnation consists of non-fossiliferous, gray, inter-laminated clay, silty clay, and fme quartzose sand. According to Marsalis and Friddell (1975), the Tuscahoma Fonnation near the Chattahoochee River, consists of90 to 153 feet ofnonfossiliferous, gray, inter-laminated clay, silty clay, and fme quartzose sand. Reinhardt and others (1994) indicate the Tuscahoma is composed of 10 to 60 feet of dark greenish-gray clay and silt inter-laminated with thin, medium greenish gray, quartz sand beds. The basal bed consists of massive clayey, fme- to medium-grained sand containing coarse quartz, glauconite and phosphate pebbles.
30

Figure 32. North dipping silty clay of the Tuscahoma Formation. Morris quadrangle.
Figure 33. Deeply weathered silty clay of the Tuscahoma Formation. Morris quadrangle. 31

Lower to Middle Eocene Claiborne Group (Tcb) The Claiborne Group is a thick, generally sandy unit that, in the current map area, lies between the
Tuscahoma Formation and the Altamaha Formation and/or the Tertiary Sediments and Residuum unit. Sandy sediments in this stratigraphic interval that are found in this part of Georgia's Coastal Plain have normally been referred to as the Tallahatta Formation (Marsalis and Friddell, 1975). These sediments are equivalent to those sandy sediments classified as the Claiborne Group in the Americus geologic atlas (Cocker, 2003) and in the Morris, Carnegie and Doverel quadrangles.
Outcrops of the Claiborne Group in the current map area are generally poor because of the soft, easily erodable nature of this material (Figs. 34- 38). As in previously mapped areas to the east (Cocker, 2003b, 2004a, 2005b, and 2006c), the Claiborne Group consists generally of massive to fmely laminated, white to light tan to brick-red, lo~ally kaolinitic, fme- t? coarse-grained sand and sandstone. Locally, ground water has stained the sand and sandstones to various shades of yellow and red. Cross-bedding and fme-scale layering may be observed in some of the more indurated, less weathered outcrops. Thin streaks of kaolin, kaolin laminae, and kaolin clasts may also be found. Thickness of the Claiborne Group ranges from 50 to 150 feet.
Because this unit is generally poorly cemented, Claiborne Group sandstones are highly susceptible to rapid erosion. Erosion of the soft sands that constitute the deeply weathered portions of the Claiborne Group is of major concern to the farmers in the area, particularly on slopes adjacent to a major drainage. Most of the slopes adjacent to the streams have been kept in a natural, forested state to curb that type of erosion. Severe erosion may threaten the integrity of the transportation and utility infrastructure, also.
Figure 34. Soft, fme-grained sandstone of the Claiborne Group. Undercutting by erosion or road grading may initiate collapse of the sandstone. Carnegie quadrangle.
32

Figure 35. Soft, fme-grained sandstone of the Claiborne Group underlies more coherent, less easily eroded Altarnaha Formation sandstone. Contact is at the dramatic change in slope. Carnegie quadrangle.
Figure 36. Gleying alteration offme-grained sandstone of the Claiborne Group. Carnegie quadrangle. 33

Figure 37. Portion of silicified tree log found near Hog Creek. Carnegie quadrangle.
Figure 38. Contact between soft sandstone of the Claiborne Group and overlying chert and clay residuwn of the Ocala Group. Contact above hammer. Carnegie quadrangle.
34

Figure 39. Chert and clay residuwn of the Ocala Group overlying soft sandstone of the Claiborne Group. Carnegie quadrangle.
Eocene to Oligocene Tertiary Sediments and Residuum (Tsr)
In the current map area, exposures of residuwn were found in the Carnegie and Doverel quadrangles (Figs. 38 - 42). Concentrations of chert rubble accompanied by abundant, predominantly maroon to brown to chocolate brown and less commonly white and orange, plastic or sticky clay is the best indication of this unit's presence. Chert and associated brown clays that are the most abundant part of this unit may be derived from intense, subaerial weathering of carbonate sediments. Outcrops of an intensely weathered sandstone (Figs. 43, 44) may belong to the Claiborne Group or this Tertiary Sediments and Residuwn unit.
Chert found in the map area ranges in size from gravel to cobbles and small boulders. Rare chert clasts found associated with Altarnaha Formation sediments may be sedimentary clasts eroded from the residuwn and incorporated into the Altamaha Formation during deposition of the Altamaha Formation (Cocker, 2004). The paucity of chert clasts within the Altamaha Formation within the current map area suggests that much of this residuwn unit was eroded prior to Altamaha deposition and/or not much chert was present in the residuwn. Examination of quadrangle geologic maps from the Americus atlas (Cocker, 2003b) and the Lwnpkin project area (Cocker, 2006c, and this year's mapping) indicate a large gap of mapped residuum. This gap extends from the western side of the Doverel quadrangle across the western side of the Dawson quadrangle as well as areas to the north of the Doverel quadrangle. This gap is centered over the
35

Ichawaynochaway Creek drainage. This gap may well represent paleo erosion of the residuum in this area by an ancestral Ichawaynochaway Creek prior to deposition of the Altamaha Formation.
Further to the east, fossils preserved within the chert-bearing residuum have been identified as Late Eocene to Early Oligocene (Summerour, 2000) or Late Oligocene (Huddlestun and others, 1974). Stratigraphic position of the residuum is permissible for Early or Late Oligocene, as well as including rocks of Middle to Upper Eocene age. Early Oligocene residuum may be derived from weathering of the Oligocene Tivola or Eocene Ocala Limestone (Summerour, 2000). Late Oligocene residuum may be derived from the Suwanee Limestone. As this residuum lies directly on the Claiborne Group (Figs. 38, 39), the source material is more likely to be from the Ocala Group.
Huddlestun and others (1974) distinguished the occurrence of chert as clasts and in situ massive chert in a similar manner to that which occurs in the current map area. Chert clasts are described as sand to gravel-size detritus, cobbles and boulders in a matrix of sand and clay. In situ chert occurs as massive bedded chert, and chert pinnacles surrounded and overlain by Neogene age sands, clays and gravels. These in situ cherts are referred to as the Flint River Formation by Pickering (1966, 1970).
Thickness of the residuum unit is quite variable, because it is derived through weathering and erosion of rock units prior to Altamaha sedimentation. Maximum thickness in the current map area is believed to be on the order of 10 feet.

Figure 40. Chert clast from the Tertiary Sediments clearing. Carnegie quadrangle.
36

during land

Figure 41. Brick-red sandstone of the Altamaha Formation (Ta) overlies light brown chert and clay residuum of the Tertiary Sediments and Residuum Unit in the left, uphill side of the photo. Reddish brown, soft sandstone of the Claiborne Group lies to the right and below the residuum. Doverel quadrangle.
Figure 42. Resistant chert residuum of the Ocala Group holds up hill along dirt road. Softer red sandstone of the Claiborne Group lies beneath of the residuum and crops out on the right side. Carnegie quadrangle.
37

.

........ r'=,

. ~

.:;

..,....,

Figure 43. Intensive kaolinization of fine-grained sandstone with several "boulders" of relatively unaltered

sandstone. These "boulders" are located by the hammer and to the left of the hammer. This sandstone may

belong to the Claiborne Group or the Ocala Group. Carnegie quadrangle.

Figure 44. Intensive kaolinization and bleaching of fme-grained sandstone with relatively unaltered sandstone. This sandstone may belong to the Claiborne Group or the Ocala Group. Carnegie quadrangle.
38

Post Upper Cretaceous- pre Miocene K- T breccia/conglomerate (K-Tbx) Several exposures of multilithic breccia, conglomerate or conglomeratic sandstone were found in the
Hatcher, Morris, and Carnegeie quadrangles. This lithology or lithologies are distinctly different from the adjacent stratigraphic lithologies. In the Hatcher and Morris quadrangles, this lithology lies beneath Nanafalia Formation sandstone and above Providence Formation sandstone. In the Carnegie quadrangle, a similar type of lithology is exposed beneath an outcrop of the Altamaha Formation. Topographically below this outcrop are exposures of the Eocene age Claiborne Group sandstone. The lithology exposed in the Morris and Hatcher quadrangles is quite similar to that previously encountered in the Georgetwon and Lumpkin quadrangles that lies above the Providence Formation and below the Paleocene age Clayton Formation (Cocker, 2007f). Based on the differences in lithologies and observed or inferred stratigraphic positions, the occurrence in the Morris and Hatcher quadrangles is believed to be older than those in quadrangles further to the east (Cocker, 2007f).
These types of lithologies are discontinuous. Those in the Carnegie quadrangle have been included as part of the Tertiary Sediments and Residuum unit as their exposures are rather limited in extent and not necessarily mappable.
The Morris and Hatcher exposures contains numerous rounded to subangular clasts of sandstone, iron oxide-cemented sandstone and kaolin sandstone (Figs. 45 - 50). The exposure shown in Figs. 45 -50 grades rapidly upward from conglomerate to clay. It is in unconformable contact with cross-bedded sandstone of the Providence Formation. It also contains unusual, botryoidal masses of iron oxide. Some are elongate, similar to stalactites (Fig. 47). None appear to be in avertical, "growth" position, and all are broken, suggesting that they did not form in situ, but were transported along with the other clasts. This type of botryoidal iron oxide has not been observed anywhere else in the Upper Cretaceous -Tertiary sediment\1-ry section ofthe Coastal Plain.
39

Figure 45. Outcrop of conglomeratic clay (K-Tbx) in unconformable contact with cross-bedded sandstone of the Providence Formation. The conglomeratic material grades upward into clay of the Clayton Formation. Angular clasts of iron-oxide cemented sandstone, botryoidal masses of iron oxide, sandstone, kaolin, and c Morris
Figure 46. Heterolithic conglomerate of angular sandstone, botryoidal goethite, and rounded to subangular kaolin clasts about 10 feet east of the previous photo and 4 to 5 feet lower in elevation. Here the conglomeratic material had cut down at least this much in elevation into the cross-bedded sandstone shown in Fig. 45. Morris quadrangle.
40

Figure 47. Botryoidal, goethite clasts common in this basal conglomerate. Morris quadrangle. 41

Figure 48. Channel sandstone of the Nanafalia Formation down cutting into Clayton Formation clay that grades down to conglomerate (K-Tbx) exposed in lower third of outcrop. Morris quadrangle.
42

Figure 49. Rapidly fming upward conglomerate consisting of abundant rounded to subangular kaolin, sandstone, and botryoidal goethite clasts in clay and sand matrix. Morris quadrangle.
43

Figure 50. Outcrop of clast-rich conglomerate approximately 0.5 miles E of the previous outcrop shown in Figs. 45 - 50. Subangular to subrounded clasts of kaolin, kaolinitic sandstone, sandstone, iron oxide cemented sandstone and light gray clay (K-Thx). Hatcher quadrangle.
Figure 51. Another exposure of clast rich conglomerate. Morris quadrangle. 44

Figure 52. Basal sandstone of the Clayton Formation with suspended clasts of gray kaolin from the underlying Providence Formation kaolin. Morris quadrangle.
Presently, the origin of these lithologies, as well as other occurrences observed during previous years of mapping, is unknown. Clast size, poor sorting, and variable angularity of the clasts suggest a relatively high energy environment. The apparent stratigraphic position of these lithologies above the top of the Upper Cretaceous Providence Formation and perhaps during the Eocene (post Claiborne and pre Altamaha), correlates roughly with possib' le high energy sedimentation related to the Late Cretaceous meteoritic impacts in the Yucatan and with the Eocene age Chesapeake Bay impact (Cocker, 2006a; 2007f).
Miocene Altamaha Formation (Ta)
Clastic sedimentary rocks of the Altamaha Formation are the youngest Tertiary rocks in the map area and are generally found at the higher elevations, particularly on the interfluve areas (Plates 2 - 6). Locally, the Altamaha Formation is present at lower elevations than its projected lower contact as was also noted by Hetrick (1992) and Nystrom and Willoughby (1982 and 1986). The Altamaha Formation has been observed in contact with the Tertiary Sediments and Residuum unit, Tobacco Road Sand, Claiborne Group, Tuscahoma, Nanafalia, Clayton, and Providence Formations (Figs. 41, 53, 55 - 59, 62 - 66, 68, 70). Elevation differences in the lower Altamaha contact, as well as cutting progressively older sedimentary
45

units to the north and west, indicate a major disconfonnity prior to (and perhaps during) Altamaha sedimentation. Also, numerous exposures show the Altamaha Formation downcutting into the older sediments.
Thickness of the Altamaha Formation is also quite variable. Maximum thickness is probably on the order of 20 to 30 feet. The Altarnaha Formation may thin to less than 10 feet in many parts of its mapped area. Indurated sandstones of the Altamaha Formation have protected underlying, softer sediments from more rapid erosion (Figs. 35, 64).
Lithologically, the Altamaha Formation consists of sandstones, argillaceous sandstones, and conglomerates. The dominant lithology observed in the current map area is a massive, brick-red, argillaceous, fme-grained to gritty sandstone. Small, rounded, generally black, ironstone pebbles may be very abundant to rare, but are usually present, especially near or at the basal contact. Thin or cross-bedding is very rarely observed. Weathering, iron staining and mottling probably mask the presence of more sedimentary structures and textures in the Altamaha Formation. A recent exposure of the Altamaha Formation in the Burke County landfill in Waynesboro (Figs. 58, 66), depicts excellent examples of crossbedded conglomeratic sandstone, as well as the more commonly observed massive, red, conglomeratic sandstones found within the STATEMAP area from the Flint River to the Chattachoochee River. In many exposures, the massive, more or less mottled, argillaceous sandstone is found beneath the brick-red sandstone, but are above other brick-red, less argillaceous sandstone.
A basal conglomerate is commonly present that is very useful for recognizing this unit's basal contact. Within the current map area, clast composition of the conglomerate generally consists of iron oxide, iron oxide-cemented sandstone, and ironstone pebbles (Figs. 53 - 69). Clasts of iron oxide were probably derived mainly from residuum of the Clayton Formation. Iron oxide-cemented sandstone clasts were probably derived from one or more underlying sandstone units that locally have iron oxide-cemented sandstone crusts (e.g. Claiborne Group, Clayton(?) and Providence Formations). Rarely, chert or kaolin clasts may be present. Chert clasts were derived from the Tertiary Sediments and Residuum unit, and the kaolin clasts were probably derived mainly from the Nanafalia Formation. Thickness of the conglomerate is generally on the order of 6 inches to several feet. Kaolin clasts are a significant feature of the Altamaha Formation in South Carolina, but their source is unknown (Ralph Willoughby, personal communication, 2007).
Altamaha Formation sandstones contain variable amounts of ironstone pebbles that generally range in size from 0.25 to 1.00 inches. Occasionally, ironstone pebbles up to 2 inches are found. Most ironstone pebbles are black and appear to be rounded to subrounded with an apparent polish. Although these pebbles were not examined by petrographic or chemical analyses, visual inspection with a hand lens suggests that these pebbles consist of clastic quartz grains cemented by a mixture of iron oxides, quartz and perhaps hardened clay. These ironstone pebbles are currently clastic in their occurrence. Generally found dispersed in a sandstone or argillaceous sandstone matrix, these ironstone pebbles are also concentrated in conglomeratic portions of the Altamaha Formation and occasionally in distinctly layered portions of the
46

Altamaha Formation (Fig. 53). Estimated abundance of the ironstone pebbles in the Altamaha Formation in the current map area ranges from 0 to 50% with the more common abundance probably in the 5 to 10% range. Weathering of the ironstone pebble-bearing Altamaha Formation concentrates these pebbles as a lag deposit on the present surface (Fig. 69). Although these ironstone pebbles have been noted from this part of the stratigraphic section over much of the Upper Coastal Plain of Georgia, no source for the ironstone pebbles has been identified. A unique occurrence of iron-oxide cemented ironstone pebbles was found in the Doverel quadrangle (Fig.54). The iron oxide is clearly of a secondary nature and cements the ironstone pebbles into a layer about 1 foot thick.
Figure 53. Layers of ironstone pebbles are visible within the base of the Altamaha Formation. Base of hammer is at Altamaha- Claiborne sand contact. Doverel quadrangle.
47

Figure 54. Iron oxide-cemented ironstone pebbles form a layer approximately 1 foot thick. Abundant ironstone pebbles are visible above and below that layer, as well as within that layer. Doverel quadrangle.
The more argillaceous sandstone may be mottled with various shades of white, yellow and red being the most prevalent (Figs. 71 -73). Where present with sandier portions of the Altamaha Formation, this mottled clay-rich lithology is always beneath the sandier portion. Although relatively indurated, this clayrich lithology is believed to be the kandic zone formed by downward mobilization of clay. The amount of clay seems to be variable throughout the current map area. Data from Long and Baldwin (1915) indicate that, despite the enrichment of clays in the subsoils (kandic zone), the rock/soil is an argillaceous sandstone based on a greater volume of sands versus silts and clays. Mottling is believed to represent remobilization and oxidation of iron and kaolin by ground water during weathering. Occasionally concentration and precipitation of iron resulted in the formation of hard black masses that are called plinthite. These pebbles have been referred to as plinthite (Summerour, 2000); however, true plinthite is actually a soft, weatheringrelated segregation of iron oxide to form irregularly shaped masses (Brady and Weil, 1999). Plinthite may be found locally developed as irregular-shaped masses in the lower portions of the kandic weathering zone.
Size analyses and descriptions of soil and subsoil for Grady sandy loam, Greenville sandy loam, Ruston sandy loam, and Tifton sandy loam soils in Terrell County (Long and Baldwin, 1915) suggest that these soils were derived from the Altamaha Formation (Cocker, 2001). As described in the section on soils, these four soil types have the same grain size distribution in the soil and subsoil. Subsoils show a second population of clay-size particles that reflect enrichment of clay in the subsurface. The upper soil zone corresponds to the more uniformly colored massive sandstone. The lower argillaceous zone corresponds to
48

the lower mottled argillaceous sandstone. In the present quadrangles, the Altamaha Formation disconformably overlies the Claiborne Group, the
Tertiary Sediments and Residuum unit, as well as the Tuscahoma, Nanafalia, Clayton and Providence Formations. This disconformity can be observed at the outcrop scale where it ranges from 1 to 20 feet (Figs. 41, 53, 55, 57- 59, 62- 66, 68, 70), from outcrop to outcrop, and at the map scale where relief may range up to about 100 feet between outcrops (Plates 2 - 5). The disconformity at the base of the Altamaha Formation marks downcutting in progressively older units to the west and north. Units mapped further to the east (Clinchfield Formation, Ocala Group, and Lisbon Formation) have been removed prior to Altamaha deposition or their lithologies are not adequately distinguishable to be separated and are included in the Tertiary Sediments and Residuum unit.
Depositional environment of the Altamaha Formation is interpreted as an irregular, prograding fluvial and estuarine system developed during the Early and Middle Miocene period of lowered sea level (Huddlestun, 1988, 1993). Prior to and during the Early and Middle Miocene, Oligocene and older sediments were exposed to intensive weathering and erosion. As a result, the lower contact of the Altamaha Formation with underlying units is highly irregular. Older units exposed to the weathering and erosion may be irregular in thickness or missing. Contact relations, irregular surface, and variable basal conglomerate clast population are consistent with the anastamosing fluvial channels suggested by Huddlestun.
Detailed mapping of the Altamaha Formation in South Carolina in and near the Savannah River Site (Fallaw and Price, 1992; Nystrom and Willoughby, 1982) contains similar lithologies and has similar geologic relations as those found in the present map area. The author examined outcrops of the Altamaha Formation in South Carolina with Ralph Willoughby in May, 2007. Although the iron oxide content is not as evident in South Carolina as the Altamaha Formation sediments shown in Figs. 53 - 68, Altamaha Formation sediments examined in South Carolina were similar to Altamaha Formation sediments examined in eastern, central and western Georgia. Variations in clast and sediment composition are evident from South Carolina to western Georgia and should be expected in fluvial environments draining the complex southeastern Piedmont.
In South Carolina and in the Burke County exposure, the Altamaha Formation overlies and cuts sediments of the Tobacco Road Sand, generally thought to be Late Eocene in age. In South Carolina, the Twiggs Clay of the Dry Branch Formation may be as young as late Oligocene to early Miocene (23.0 +/0.2 my) based on a Rb-Sr isochron of glauconite (Harris and Fullagar, 1982. The basal Tobacco Road Sand may be late Oligocene or early Miocene based on archaeobalanid barnacles (Zullo and others, 1982).
Pollen found in massive, sandy clay and clay beds in upland deposits overlying Cretaceous sediments in the Americus 30' x 60' quadrangle is believed to be no older than Miocene (Reinhardt and others, 1994). Although not examined by this author, these sediments are believed to be equivalent to the Altamaha Formation.
49

Figure 55. Channel of the massive, brick-red, pebble-rich conglomeratic sandstone of the Altamaha Formation cutting into reddish brown sandstone of the Providence Formation. Morris quadrangle.
Figure 56. Basal cobble conglomerate of the Altamaha Formation overlying sandstone of the Claiborne Group. Morris quadrangle.
50

Figme- 57. Channel of Altamaha Formation sandstone- cut into soft sandstone of the- Claiborne Group sandstone-. Base of channel is marked by the shadow of the overhanging more resistant Altamaha Formation and the hammer. Doverel quadrangle.
.Figme 58. Large sheam channel of Altamaha Formation cut into Eocene-age? Tobacco Road Sand. Channel is about 150 feet wide and cuts down to about the base of the pit. Location is the Burke County landfill in Waynesboro, Ga.
51

-~!~t!!f.,C:11~'~~~~~ ..., ~ :-

~--- d

Figure 59. Lower contact of Altamaha Formation marked by boulder conglomerate. Clasts are iron oxide-

and silica-cemented sandstone probably derived from the underlying Claiborne Group. Brooksville

Figure

marked by pebble bed that cuts across apparently massive

sandstone. On the left of the outcrop, pebble bed is about halfway up outcrop and begins to cut down to

near base of outcrop by tree. Morris quadrangle.

52

.

. . ..

,._ .>~ ---~--:: <:-~'_;,~-;~::::_,,~-:-,--:::~'-_.;:~;-.l.'~;~~(_ -~; ,t-1_: - ;~-: _ : -.:_,

Figure 61, Right side of channel shown in Fig. 60. Pebble bed is more visible in this photo. Morris quadrangle.

Figure 62. Channel edge of conglomeratic sandstone of the Altamaha Formation cuts down into softer sandstone of the Providence Formation. Hatcher quadrangle.
53

Figure 63. Brick-red conglomeratic sandstone cuts several channels into underlying brown sandstone of the Nanafalia Formation. Monis quadrangle.
Figure 64. Basal megaclast conglomerate of the Altamaha Formation overlying soft sandstone of the Claiborne Group. Large clasts are iron oxide-cemented sandstone from the Claiborne Group. Contact is located at the abrupt change in slope where the hammer is located. Doverel quadrangle.
54

Figure 65.

of pebble-rich conglomerate of Altmnaha Formation cutting underly-ing Nanafalia

Formation sandstone. Morris quadrangle.

Figure 66. Cross-bedded basal conglomeratic sandstone of the Altamaha Formation cuts underlying Tobacco Road Sand. Location is Burke County landfill in Waynesboro, Ga.
55

Figure 67. Ironstone and quartz pebble conglomeratic sandstone at same stratigraphic horizon as in Fig. 66. Cross-bedding textures were obliterated by clays and iron oxide staining. Location is Burke County landfill in Waynesboro, Ga.
Figure 68. Subtle, west-dipping contact between the semi-polygonal jointed sandstone of the Altamaha Formation overlying the more massive Nanafalia Formation. Morris quadrangle.
56

Figure 69. Lag pavement of ironstone pebbles sandstone. Doverel quadrangle.

bleached Altamaha Formation

I I
J
Figure 70. Basal chert clast conglomerate at Altamaha Formation- Tobacco Road Sand contact. Southwest of Sandersville, Ga.
57

Figure 71. Increasing downward mottling of Altamaha Formation sandstone. Mottling involves downward migration of iron and aluminwn to form kaolin and iron oxide-cemented sandstone. Morris quadrangle.
Figure 72. Increasing downward mottling of Altamaha Formation sandstone. Mottling involves downward migration of iron and aluminwn to form kaolin and iron oxide-cemented sandstone. Carnegie quadrangle.
58

Figure 73. Mottled zone in Tobacco Road Sand cut by cross-bedded, basal conglomeratic sandstone of the Altamaha Formation. Upper mottled zone is developed near the present top of the Altamaha Formation and is clearly separate from the underlying basal pebble conglomerate, as well as the underlying mottle zone in the Tobacco Road Sand. Location is the Burke County landfill in Waynesboro, Ga.
Quaternary Tertiary - Quaternary Alluvium (TQal)
River terraces that may be present adjacent to the Chattahoochee River north of the Hatcher quadrangle are not present on the Georgia side of the river. Potential terraces that were suggested north of the Hatcher quadrangle are about 10 to 30 feet above the present level of the Walter F. George Reservoir. The lowermost area, adjacent to the river is defmed as being the current flood plain and capped by Quaternary alluvium- essentially alluvial material deposited by the river at or near its more recent elevation.
One outcrop of a conglomerate-filled channel (Fig. 74) cuts the Providence Formation sandstone at an elevation of 300 feet and approximately one mile east of the Chattahoochee River. Large subangular to subrounded clasts of iron oxide-cemented sandstone are found in this channel. This channel does not resemble any exposures of the Altarnaha Formation or other mapped unit. This exposure may represent a Pliocene-age? upland stream channel.
59

Figure 74. Unusual, high level, conglomeratic channel fill. Hatcher quadrangle.
Quaternary Alluvium (Qal)
Alluvium was mapped as occupying the basal, generally flatter portions of creek valleys in the map area. Alluvium was mapped as extending up the smaller tributaries where a stream occupied the valley and the valley could be recognized as a valley on the topographic map. Areas depicted as marsh on topographic maps, especially those on the Doverel quadrangle, are mapped as alluvium. When the Doverel quadrangle was mapped a severe drought was in effect, and these areas, as well as many of the areas depicted as ponds, were dry.
Except for minor exposures along stream banks, no outcrops were observed. Alluvium is described as consisting of variably micaceous, poorly-sorted sand, clayey sand, and clayey silt, with a minor amount of quartz and local chert gravel, and variable amounts of organic matter. The generally larger expanses of swampy areas in the present map area suggest a greater portion of organic matter may be present than in areas further to the east (Summerour, 1999, 2000). Thickness of alluvium is variable and is probably greater in the major creek valleys (i.e., Carter, Ichawaynochaway, Cemochochechobee, Hog, Pataula, Holanna, Hodchodke Creeks, South Fork ofTobanee Creek, and Drag Nasty Creeks) as well as adjacent to the Chattahoochee River.
60

Alluvial terraces that were formed during downcutting of the creeks may be present but are not recognizable by their topographic expression on the topographic maps of these quadrangles or in the field mapping. The soft, easily erodable nature of the sediments in the Claiborne-Group, Tuscahoma, Nanafalia, and Providence Formations would tend not to preserve a recognizable terrace.
Alteration of primary sedimentary textures and evidence of previous groundwater movement
Most of the outcrops of Coastal Plain clastic rocks observed during the mapping of the past several years do not display primary sedimentary textures. This is particularly apparent in those rocks that are dominantly red or reddish brown in color. Alteration of clastic rocks, particularly through groundwater movement and deposition of iron oxides that stain the rocks various shades of red, yellow and brown, appears to obliterate the appearance of primary sedimentary textures. Evidence of past ground water activity is apparent in iron oxide-cemented and iron-stained sediments, as well as mottled sediments. Several episodes of groundwater movement were observed in at least one exposure (Fig. 73). The mottled zone shown in the Tobacco Road Sand is cut by the basal conglomerate of the Altamaha Formation. Another mottled zone is present at the top of the exposed Altamaha Formation. Mottled zones are developed where near surface clays and dissolved iron have migrated downward and concentrated at some depth, the mottled zone shown at the top of the Altamaha Formation represents a weathered zone that has subsequently been exposed by erosion.
Kaolin and iron oxide mineralization associated with joints record multiple episodes of groundwater movement along these joints. Cross-cutting joints indicate other periods of groundwater movement. Fig. 89 depicts a multistage joint cutting paleo mottling in the Nanafalia Formation.
Correlation of STATEMAP map units with nearby 1:100,000 scale maps and the 1:500,000 scale Geologic Map of Georgia
On the 1:500,000 scale Geologic Map of Georgia (Georgia Geologic Survey, 1976) the map units which lie within the current map area are the Ripley (Kr), Providence (Kp), Clayton (Pel), and Nanafalia (Pnf) Formations, the Clayton, Porters Creek and Nanafalia Formations undifferentiated (Pen), Tuscahoma Sand (Ptu), Claiborne undifferentiated (Be), and Eocene and Oligocene residuum undifferentiated (Eo-M). On the Geologic Map of Georgia, several of these formations (Clayton and Nanafalia formations plus the Porters Creek Clay) are combined as an undifferentiated unit (Pen) because of difficulties in distinguishing these units in the field. A plot of the Digital Geologic Map of Georgia (Cocker, 1999a) relative to the currently mapped geology of the current map area illustrates a relatively good agreement of the two sets of maps. The principal differences lie in the mapping of Quaternary alluvium in stream valleys, mapping of the Altamaha Formation (Ta), and :rertiary Sediments and Residuum (Tsr) generally in the stratigraphic position of the Eocene and Oligocene residuum undifferentiated (Eo-M) on the Digital Geologic Map of
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Georgia (Cocker, 1999a), and the attempt in this project to separately map the lower Tertiary strata. Spatial differences are related to the reconnaissance scale mapping that produced the Geologic Map of Georgia (Georgia Geologic Survey, 1976), stretching the usable scale of the Digital Geologic Map of Georgia (Cocker, 1999a) to that of the 7.5 minute quadrangles, and to errors created during production of the Digital Geologic Map of Georgia (Cocker, 1999a).
BIOSTRATIGRAPHY
Outcrops of Tertiary age sediments in the present map area are generally nonfossiliferous. Chert residuum within the Tertiary Sediments and Residuum unit and chert clasts in the Miocene Altamaha Formation are locally fossiliferous in the present map area. In occurrences of this chert further to the east, fossils were identified as Late Eocene, Early Oligocene, and Late Oligocene (Huddlestun and others, 1974; Swmnerour, 2000).
Trace fossils, in the form of Ophiomorpha burrows, are found within sandstone of the Providence and Nanafalia Formations. Burrows are generally lined with kaolin and apl'ear to have kaolin cementing sand within the burrows. Those burrows are on the order of 1 to 1.5 inches in diameter and have a thicker kaolin lining. Overall length of individual burrows found in the Providence Formation in the Lumpkin quadrangle may be on the order of several feet and appear to branch (Cocker, 2004). Burrows are generally straight to slightly curved. These burrows may have been built by a clam or crab. This type of trace fossil within shallow or nearshore marine sediments is classified as belonging to the Skolithos ichnofacies of trace fossils (Frey and Pemberton, 1984). These trace fossils are useful as a paleoenvironmental indicators but are not unique to a particular time interval.
The Ripley Formation is normally a relatively highly fossiliferous stratigraphic unit, but fossils were absent in the exposures observed in the current map area. A summary of the fossils noted by Almand (1961) is included in Cocker (2004).
Petrified wood was found by a local property owner in the Carnegie quadrangle near Hog Creek (Fig. 37). The petrified wood shown in that figure represents a rather large tree. The original log was approximately 12 feet long. A rough estimate of the original diameter of the tree would be at least 5 feet.
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STRUCTURAL GEOLOGY.
Although Southeastern Coastal Plain sediments are connnonly believed to have undergone little or no structural modifications since deposition, there is an increasingly voluminous body of literature that documents numerous structures that record a surprising number of events. During the past decade, studies in and around the U.S. Department of Energy (USDOE) Savannah River Site, Aiken, SC have resulted in the recognition of eight major regional structural events during early phases of rifting related to Triassic - Jurassic opening of the Atlantic Ocean and ten major events since Late Cretaceous passive margin sedimentation (Bartholomew and others, 2007). Especially significant are Late Eocene, Late Miocene, and Late Quaternary events that are marked by significant surface deformation and erosion. Both reverse and normal faults are recognized by Bartholomew and others (2007). Many of these faults appear to represent reactivation of joints. Both joints and faults appear to represent multistage events. A large selection of studies documenting these structures is provided in Bartholomew and others (2007). Other reports by Cofer and Fredericksen (1982), Cofer and Manker (19983), Cofer and others (1976), Cocker (2003a, 2003b, 2004b, 2005b, 2006c, 2007c, 2007e), Prowell (1983, 1988), Reinhardt and others (1984), Sever (1966), indicate widespread structural activity affected many parts of the Georgia Coastal Plain. Lineaments in aeromagnetic data that cut and offset aeromagnetic contours in Georgia's Coastal Plain (Daniels, 2000) are indications of large scale, deeper faults. One of these lineaments spatially correlates with the Andersonville fault and extends it much further to the east and west (about 40 miles). Regional structural data that focused on faults (Prowell, 1983, 1988) indicate deformation extended throughout the Gulf and Atlantic Coastal Plains. Documentation of structural information in the Coastal Plain is critical to understanding aquifer integrity, landfill siting, continuity of sediment hosted mineral deposits of kaolin, bauxite, attapulgite, and phosphates, and siting of nuclear facilities.
In contrast with rocks found in the Valley and Ridge, Blue Ridge and Piedmont geologic provinces of Georgia, sediments of the Georgia Coastal Plain are both difficult to map and are poor hosts for the preservation of structures, particularly faults. Many Coastal Plain exposures are massive with bedding connnonly masked or obliterated by remobilized clays and iron oxides, particularly in the near-surface environment. Where preserved, bedding or unit contacts may show the effects of faulting or folding. In addition, faults are planes of weakness that allow passage of ground water that facilitates alteration and deterioration of the fault zone. Fresh exposures of structures in soft sediments disintegrate rather rapidly, with some changes evident on a daily basis. Joints in Coastal Plain sediments are connnonly filled with secondary clays and iron oxides and are thus less susceptible to weathering and erosion. In addition to structures noted during the current mapping, several important exposures that provide critical structural information regarding tectonic events in the Coastal Plain were found and documented during this past year. One exposure occurs in the previously mapped County Line quadrangle (Cocker, 2005b). Another important exposure is located in the eastern part of the Coastal Plain and involves the Altamaha Formation and the underlying Tobacco Road Sand. The writer is grateful to Rick Eppenheimer who alerted the writer to the exposed critical relations at the Burke County landfill near Waynesboro.
As observed during the previous years' mapping, scattered occurrences of structural deformation were found in
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the current map area. Structural deformation observed during this year's mapping includes folding, faulting, jointing, and reversal of bedding (Figs. 75 - 92). As with all potential observations of deformation, the following conditions must be present: deformation, bedding or formational contacts that allow the deformation to be observed, and exposure of the deformation. Within the current map area, with the exception of cross-bedding, bedding was generally poorly exposed, developed, or preserved. Larger scale deformation may be present, but could not be well documented because of the lack of subsurface data. Outcrop scale deformation was observed in the Carnegie and Morris quadrangles.
Folding is best displayed by thin-bedded sandstone beds in the Providence Formation (Fig. 91). Outcrops of folds observed during the previous years' mapping (Cocker, 2003a, 2003b, 2004b, 2005b, 2006c, 2007c, 2007e) suggest folding has affected bedding in the Providence, Clayton, Nanafalia, and Tuscahoma Formations and the Claiborne Group. Folding may have affected the Altamaha Formation (Miocene). Folding may have occurred at different episodes during the Tertiary (Bartholomew and others, 2007) or during one event. Axis of the fold shown in Fig. 92 is 300 (unpublished data courtesy of Rick Eppenheimer, 2007). That fold affected only the Tobacco Road Sand and is clearly older than the erosion at the base of the Altamaha Formation as well as deposition of the Altamaha Formation.
As regional dips in this part of the Coastal Plain are to the southeast, bedding dips that are reversed and dip to the north and/or to the west are anomalous. On the outcrop scale, bedding reversals indicate more and possibly larger scale folding is present. In most instances, the entire fold structure or strata on the opposites hinges of the folds are not exposed. Thinly bedded clays of the Tuscahoma Formation in the southern part of the Morris quadrangle (Fig. 32) display a consistent dip to the north.
Several faults were observed during this year's mapping (Figs. 75 -78). The general trend of these structures is NNW. The amount and direction of displacement on these structures is generally unknown. Several faults that form a graben-like structure were observed in the County Line quadrangle (Figs. 80 - 83). Sandstone of the Claiborne Group is down-dropped approximately 10 feet relative to sand and clay of the Tuscahoma Formation. A drag fold is observed adjacent to the graben (Fig. 81). Prowell (1983, 1988) noted that many of the faults in the western part of the Coastal Plain are grabens or parts of grabens (Fig. 9_3). The fault shown in Figs. 84 and 85 has an azimuth of 305 (unpublished data courtesy of Rick Eppenheimer, 2007) and has the same orientation as a group of joints reported by Bartholomew and others (2007).
Jofuts were generally found within the Providence, Nanafalia and Altamaha Formations. The joints record previous movement of ground water with formation of kaolin and iron oxide in or adjacent to the joints (Figs. 86 89). Cross-cutting joints record several episodes of jointing and ground-water movement along those joints. The large joint shown in Fig. 87 is approximately 1.5 feet in width and may well have been reactivated as a fault. The joint shown cutting the Providence Formation in Fig. 88 is cut by the overlying Nanafalia Formation sandstone. Clearly, jointing occurred after the Providence was buried but prior to erosion and subsequent deposition of the overlying Nanafalia Formation sandstone. As the joints shown in Fig. 89 clearly cut the mottling, the mottling was probably developed in an older, near surface weathering environment, subsequently buried and subjected to stresses that caused the later jointing.
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In the Springvale district, Clark (1965) noted the presence of numerous small faults having displacements of up to 20 feet. U.S. Bureau of Mines drilling indicated vertical dislocations of the Tuscahoma- Nanafalia contact up to 40 feet within a horizontal distance of 100 feet. Unfortunately, documentation of the drill data and evidence for the numerous small faults were not included in Clark (1965) or on his geologic map.
Figure 75. Normal fault with bedding dipping in opposite directions. Carnegie quadrangle.
65

Figure 76. Faulted contact between brick-red sandstone of the Altamaha Formation and clay of the Tuscahoma Formation. Morris quadrangle.
Figure 77. Faulted contact between kaolin and sandstone of the Nanafalia Formation. Morris quadrangle. 66

Figure 78. Deeply weathered fault within the Nanafalia Fonnation. Morris quadrangle.
Figure 79. Fault with Altamaha Fonnation on left and on top of Nanafalia Formation kaolin overlying Clayton Formation clay and iron oxide residuum on right. Morris quadrangle.
67

Figure 80. Faulted contact of the Claiborne Group sandstone overlying the Tuscahoma Formation clay. The sense of movement is down to the right or east. The soft nature of these sediments will result in this exposure disappearing after a few years either due to erosion, mass wasting or vegetation growth. County Line quadrangle.
Figure 81. Drag fold developed in sediments of the Tuscahoma Formation and overlying Claiborne Group adjacent to a graben structure at the extreme left of the photo (dark red). Lighter brown sandstone of the Claiborne Group is overlain by the darker red sandstone of the Altamaha Formation. The darker red portion of the Claiborne Group sandstone on the left may have resulted from increased porosity and permeability associated with the graben faulting. County Line quadrangle.
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Figure 82. Graben structure shown at the extreme lef' t in Fig. 79. The light inward d"i'pping planar features are the edges of the graben. Tuscahoma Formation sands are present on either side of the graben. A major slide has changed the appearance of the central part of this graben from that of Fig. 79. County Line quadrangle.
69

Figure 83. Closeup view of the right side of the graben structure shown in Figs. 79 and 80 suggests a downward bifurcation of this fault. County Line quadrangle.
70

Figure 84. NW striking fault developed in Altamaha Formation and underlying softer Tobacco Road Sand. Burke County landfill in Waynesboro, GA. Photo courtesy of Rick Eppenheimer.
Figure 85. Same structure viewed several years later after landfill pit has been partially filled. Base is more than halfway up the side of the earlier photo, and outcrop has deteriorated. Burke County landfill in Waynesboro, GA.
71

Figure 86. Multistage jointing with associated kaolinization and bleaching of the surrounding Nanafalia Fmmation

sandstone. Morris quadrangle.

I'



Figure 87. Large N-S trending joint or fault? (dark brown) cutting north dipping sandstone and kaolinitic sandstone of the Nanafalia Formation. Morris quadrangle.
72

Figure 88. Joint cutting Providence Formation sandstone beneath unconformity with Nanafalia Formation sandstone. Morris quadrangle.
Figure 89. Iron oxide stained joint cutting older mottled sandstone of the Nanafalia Formation. Morris quadrangle.
73

Figure 90. Unusual vertical structure cutting Nanafalia Formation sandstone. Interior of this structure contains clasts of kaolin, iron oxide cemented sandstone, and sandstone in a sandy silt matrix. Morris quadrangle.
74

Figure 91. Synclinal fold developed in Providence Formation sandstone. Morris quadrangle.
Figure 92. Large anticlinal fold developed in Oligocene-age (?) Tobacco Road Sand and which is cut by fluvial sandstone and channel sands of the Miocene-age Altamaha Formation. Center of fold is at the rockfall in the center of the pit. The large Altamaha Formation channel shown in Figure 58 is to the left of the photo behind the bulldozer. Burke County landfill in Waynesboro, GA. Photo courtesy of Rick Eppenheimer.
75

~ ~-
Florida
Figure 93. Map of Cenozoic faults in the Southeastern Coastal Plain and Piedmont. Many of the faults shown in Alabama are a result of subsurface drilling and seismic work related to hydrocarbon exploration and development. The paucity of structures shown in Georgia may be the result of a lack of similar subsurface data rather than an actual lack of structures. Modified from Prowell (1983, 1988).
ECONOMIC GEOLOGY The principal type of ore deposit occurring within the present map area consists of bauxite and high alumina kaolin in the Springvale bauxite district. The western side of this district extends an unknown distance into the Morris quadrangle from the adjacent Cuthbert quadrangle (Cocker, 2006c). No named mines were documented within the Morris quadrangle (Clark, 1965). Bauxite was discovered in 1916 and recorded mining lasted unti11922.
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Production was about 16,000 tons of bauxite (Clark, 1965). Smith (1929) briefly examined exposures, and in 1943 the U.S. Bureau of Mines conducted a limited shallow drilling program in the area east of the Gamer mine. The U.S. Geological Survey mapped the district and surrounding areas in 1942 and 1943. Results of these investigations are described by Beck (1944) and Clark (1965). Beck provides chemical analyses of intercepts from some of the 388 holes. It would appear that only those holes that contained visible bauxite were analyzed. Drill logs were not published, and it is thought by this writer that kaolin and probably kaolinized bauxite, bauxitic kaolin or high alumina kaolin were overlooked and not analyzed. The previous mapping and drilling program focused only on bauxite ore bodies and in a relatively small area of the district. The Andersonville district was viewed in a .similar way before it was realized that high alumina materials included various types of kaolin and mixtures of kaolin and bauxite. As a result, significant portions of the Andersonville district have been explored and mined (Cocker, 2006c).
The U.S. Bureau of Mines drilling method was by power auger, and results were apparently contaminated by sand. Clark (1965) and Beck (1944) indicated that the alumina could be increased by 5% and silica decreased by 5% to get a more accurate assessment. In assessing the bauxitic ores, the greatest intercept was 49 feet, and the largest deposit was 200 feet long and 50 to 90 feet wide (Clark, 1965). Suggested indicated and inferred reserves of bauxite were on the order of 50,000 to 150,000 long tons of all grades of bauxite (Clark, 1965). That author considered that to be a rough estimate because of the complex nonmarine stratigraphy and faulted nature ofthe Nanafalia Formation in this district.
This and previous years' mapping and drilling would also suggest that the district's geology is complex. Folding is also a consideration and apparently not recognized by the earlier geologists. A plot of bauxite occurrences recorded by Clark (1965) and during this mapping may suggest that the bauxite may occur topographically in the upper and lower parts of the Nanafalia Formation; Exploration ofjust the upper occurrences may fail to ascertain the total potential of the district. Geochemical analyses for drill holes and pit samples are documented by Cocker (2006). Mapping revealed a number ofunreported occurrences of kaolin (Figs. 29, 30, 94, 95).
Mapping in the Hatcher quadrangle indicates a probable widespread resource of coarse gravel. Grain size of the gravel ranges from about 0.5 to 4 inches. This gravel is exposed in many roadcuts in this quadrangle particularly east of State Highway 39. Some of these exposures are shown in Figures 6 - 12. In addition to being a rather rare occurrence of coarse construction-grade material in the Coastal Plain, a rail line is present and barge transport could be available on the Chattahoochee River.
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Figure 94. Kaolin and kaolinitic sandstone within sandstone of the Nanafalia Formation. Morris quadrangle.
Figure 95. Nanafalia Formation kaolin unconformably overlain by Altamaha Formation sandstone. Morris quadrangle.
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HYDROGEOLOGY
Aquifers present in the current map area include the Claiborne, Clayton, and Cretaceous aquifers. Sedimentary units that contain the regionally important Upper Floridan aquifer were not found or recognized in the present mapping or in the lithologic logs of previously drilled wells. Ocala Group limestones that are present to the east and southeast of the present study area contain the Upper Floridan aquifer (Cocker, 2003b, Swnmerour, 2000).
Claiborne Aquifer
The Claiborne aquifer is composed of Claiborne Group sediments. Claiborne Group sediments increase in thickness to the south and southeast. These sediments are absent in the Hatcher and Eufaula South quadrangles, are only present at high elevations in the southeastern part of the Morris quadrangle. Where exposed in the current map area, they are partially eroded. Erosion prior to Altamaha deposition has also reduced the thickness of the Claiborne Group. Thickness of the Claiborne aquifer in Randolph and Clay counties is reported to be mainly less than 100 feet (McFadden and Perriello, 1983) and is typically at or less than 50 feet from the surface in the Doverel and Carnegie quadrangles. Recharge occurs principally through exposures of the Claiborne Group sediments in the interfluve areas or through Quaternary alluvium.
The Claiborne Group sediments are relatively porous and permeable with soils rapidly drained of moisture during drought conditions. Permeability measurements of surface exposures of the Claiborne sediments are reported by Beck (1982). Permeability decreased in the more argillaceous portions of the Claiborne sediments and in outcrops annored by secondary clays. Water quality, transmissivity and potentiometric surface data for the Claiborne aquifer through 1982 are available in McFadden and Perriello (1983}. Water quality, potentiometric surface and water use data through 1986 are provided by Long (1989).
This aquifer is locally confined by overlying clay-rich zones in the Altamaha Formation or clay-rich residuum of the Tertiary Sediments and Residuum map unit (Figs. 38, 39). The Tuscahoma Formation, where present, serves as the underlying aquiclude. Agricultural irrigation and private residential wells are probably the principal users of the Claiborne aquifer. Some of the agricultural wells probably extend into the underlying Clayton aquifer, also.
Clayton Aquifer
The Clayton aquifer is conf'med principally to permeable limestones within the Clayton Formation. Within the current map area, the exposed Clayton Formation is represented mainly by a few exposures of relatively impermeable, clay residuum. Surface recharge into the Clayton Formation is probably minimal because of its extremely (if any) limited surface exposure. Thickness of the Clayton aquifer is estimated to be about 100 feet in the Cuthbert area and increasing to 200 feet in the southeastern comer of Randolph County. Depth to the Clayton ranges from about 250 feet in the Cuthbert area to about 350 feet in the southeastern comer of Randolph County. These thicknesses and depths are based on data in McFadden and Perriello (1983}.
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Areas in the eastern and southern parts of Randolph, which include Cuthbert and Shellman, were reported to have high yields from the Clayton aquifer in the past (McFadden and Perriello, 1983). Water from a Cuthbert city well contained 39 ppm calcliwn, 1.4 ppm sodiwn, 147 ppm bicarbonate, and a specific conductivity of 254 micromhos (Wait, 1960). Declines in water levels of the Clayton aquifer in the Cuthbert area were primarily attributed to rates of pumping and precipitation (Clark and others, 1984). Water quality of wells at Cuthbert reported by Clark and others (1984) are similar to that reported by Wait (1960). Water quality, transmissivity and potentiometric surface data for the Clayton aquifer through 1982 are available in McFadden and Perriello (1983). Water quality, potentiometric surface and water use data through 1986 are provided by Long (1989).
Cretaceous Aquifers
In the map area, aquifers below the Clayton aquifer include the Eutaw, Blufftown, Cusseta, and Providence aquifers. Aquifers below the Providence aquifer are not important ground-water sources in the current map area because of greater expenses for well construction, problems of water quality (McFadden and Perriello, 1983), and much of the Eutaw, Blufftown, and Cusseta Formations appear to be relatively impermeable marl. Analyses of water from the base of the Eutaw Formation obtained from the Georgetown city well contains high levels of sodium (123 ppm), bicarbonate (319 ppm), and specific conductivity (497 micromhos) and is unsuitable for irrigation (Wait, 1960). Even the Providence Formation contains water that is marginally suitable for irrigation. Water from the Providence Formation in a well at Ft. Gaines contained 90 ppm sodiwn, 226 ppm bicarbonate and a specific conductivity of 403 micromhos (Wait, 1960). Measurements of pH in these two wells are also rather high, 8.5 for Georgetown and 8.3 for Ft. Gaines. High sodium values in the Cretaceous aquifers are attributed to leaching of sodium from abundant feldspar in these strata, as well as connate salt water.
A significant portion of the Hatcher and Morris quadrangles consists of exposed Providence Formation. Because much of the Providence Formation appears to be permeable sand, recharge of this aquifer would be significant. Subsurface data for the Providence Formation, which forms the Providence aquifer, is inadequate to provide a reasonable picture of this aquifer in the current map area. Some ground water communication may exist further down dip between the Providence and Clayton aquifers (McFadden and Perriello, 1983). During the current severe drought, the Providence could become a source of water for irrigation.
GEOLOGIC HAZARDS
Several important geologic hazards that were observed during the present mapping involve soft, commonly unconsolidated sands, soft sandstone, and locally soft clays. Soft sands are found mainly in the Providence Formation and in the Claiborne Group. Soft clays are found in the Clayton and Tuscahoma formations, as well as Tertiary Sediments and Residuum unit.
Principal hazards in areas underlain by soft sand include rapid erosion of fannland, roadways, and undercutting and collapse of stream and road banks. Most fannlands are developed on soils overlying the Altamaha Formation. More indurated portions of the Altamaha Formation prevent rapid erosion of those soils. Rapid erosion of sandier soils
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on hillsides underlain by the Claiborne Group and the Providence Fonnation may initiate gullying. Headward erosion may encroach into the overlying Altamaha Fonnation and the soils developed on top of that unit. Generally, as the slope becomes steeper, erosion and gullying becomes more rapid. Many of the hillsides adjacent to stream valleys have been left to grow as forested land to help prevent erosion. Roadways that run down to creek and river valleys and drainage ditches adjacent to the roadways serve to channel runoff and are particularly susceptible to erosion where they are underlain by the Providence Fonnation or Claiborne Group sands (Figs. 96, 97). Where the roadways are paved, the drainage ditches may be cemented. In other places, miscellaneous material such as recycled concrete blocks, tires, kitchen appliances, etc. have been placed in those ditches to slow the runoff and resulting erosion. At several places adjacent to paved roads, drainage from the roadways has caused or exacerbated severe erosion. Vertical erosion is as much as 15 to 25 feet. Such erosion may cause catastrophic collapse of the adjacent road. The cliff-like erosional escarpment caused by headward erosion of the Providence Fonnation and Claiborne Group may also be extremely hazardous to hunters or livestock that may come suddenly upon a 15 to over 30 foot cliff.
Storm runoff from high~ay culverts (Figs. 961 97), poor irrigation or logging practices can lead to significant and rapid erosion of the soft sands in areas underlain by the Providence Formation and Claiborne Group. Culverts concentrate the flow of storm runoff. Broken, unattended irrigation pipes may pump a large flow of water into a stream drainage that is nonnally in equilibrium. Complete clear-cutting and stripping or burning of fragile ground cover in sandy terrain significantly inhibits regeneration of the ground cover that protects the sand from erosion. Erosion and undercutting of stream banks may be especially hazardous where structures or infrastructures such as gas, water and sewer pipelines are exposed may cause these pipelines to collapse and rupture. Buildings that are placed on the edges of stream banks are also subject to erosion and undercutting of the stream banks. Areas that have been built up and paved over are more susceptible to increased runoff, erosion and stream bank undercutting. The box culvert shown in Fig. 98, has been undercut and a portion of this culvert and the overlying material has slumped downward several feet. This collapse and a lack of funding resulted in this road being closed for an extended period.
Sediments eroded from uplands naturally moves downhill and affects streams and infrastructures. Erosion of the soft Providence sandstone resulted in a drainage culvert beneath a railroad track being filled with sand (Fig. 99). Eventually, the sand will fill the area shown and cover the tracks as shown in Fig. 100. Sedimentation or silting up of streams by sand eroded from the surrounding terrain reduces the depth and velocity of nonnal stream flow (Figs. 101, 102). Many stream valleys in the current map area are now dominated by broad swamps (Figs. 103, 104).
Gullies resulting from this erosion tend to collect a variety of trash (Figs. 105-107). Some of the trash, such as old tires, may be initially placed there in an attempt to prevent further erosion: This practice tends to attract additional trash, as the gullies are perceived to be a convenient place to be rid of old appliances, batteries, containers of agricultural herbicides and pesticides. The Providence Formation and Claiborne Group are both important local and regional aquifers in the southwestern Coastal Plain of Georgia. The various forms of trash may leak chemicals into these aquifers and have a detrimental effect on domestic, agricultural, and public water supplies.
Soft clay of the Clayton and Tuscahoma formations, as well as the Tertiary Sediments and Residuum unit are a geologic hazard especially when the clay is wet. The most frequently encountered hazard is on unpaved roads where slippery conditions may send a vehicle off course into a ditch, tree or another vehicle. Rutted, dried out clay is also
81

hazardous, as the ruts may also send a vehicle out of control or a vehicle may high center on a rut. Logging trucks commonly use roads in this area, and their heavy loads cause abnormally deep ruts. Local govenunent, e.g. county, road graders are frequently needed to.smooth out the ruts. As most roads that cross these formations in the current map area are paved, the Clayton and Tuscahoma formations are a relatively minor hazard. The clay-bearing Tertiary Sediments and Residuum unit is locally a problem in the Carnegie and Doverel quadrangle because of road construction and more unpaved roads that cross the residuum
Figure 96. Erosion gully developed in soft Providence Formation sandstone. Nick point is at Nanafalia- Providence Formation contact. Left edge of gully is about 5 feet from paved county road. Morris quadrangle.
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Figure 97. Erosion gully developed in soft Providence Formation sandstone. Left edge of gully is about one foot from paved county road. Morris quadrangle.

Figure 98. Eros

undercutting of soft Claiborne Group sandstone leads to ....v . ....,..,,....

paved county road. Hog Creek in Carnegie quadrangle.

83

.. ..~ -~~
Figure 99. Erosion of soft Providence Formation sandstone leads to sedimentation and filling of storm culvert under railroad tracks. Eventually this may fill up and cover tracks. Morris quadrangle.
84

I

~.. )

Figure 100. Erosion of soft Providence Formation sandstone leads to sedimentation and covering of railroad tracks.

Pile of sand on left is from die clear i:n of the tracks. Morris

Figure 101. Sedimentation results in shallowing and infilling of streams. Morris quadrangle. 85

water
Figure 103. Formation of stagnant ponded water and drowning of vegetation. Cemochechobee Creek, Carnegie quadrangle.
86

Figure 105. Erosion gullies develop into illegal trash disposal sites that may contaminate the Claiborne aquifer. Carnegie quadrangle.
87

Figure 106. Erosion gullies develop into illegal trash disposal sites that may contaminate the Claiborne aquifer. Carnegie
Figure 107. Erosion gullies develop into illegal trash disposal sites that may contaminate the Claiborne aquifer. Carnegie quadrangle.
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SUMMARY
Geologic mapping of the Carnegie, Doverel, Eufaula South, Hatcher, and Morris quadrangles (Plates 1 to 5) show the interpreted distribution of Cretaceous, Tertiary and Quaternary sediments. Exposed stratigraphic units in
'
these quadrangles consist of the Upper Cretaceous Ripley and Providence Formations, Lower Paleocene Clayton Formation, and Upper Paleocene Nanafalia Formation, Upper Paleocene to Lower Eocene Tuscahoma Formation, Middle Eocene Claiborne Group, residuum of possibly Eocene and Oligocene sediments (Tertiary Sediments and Residuum), and the Miocene Altamaha Formation. Occurrences of a post Upper Cretaceous Providence Formationpre- or syn-Lower Paleocene breccia/conglomerate and a similar pre-Miocene- post Eocene breccia/conglomerate have been located. Quaternary alluvium is found in stream valleys and the Chattahoochee River valley.
Episodes of exposure, weathering, and erosion followed the deposition of: 1) Upper Cretaceous Providence Formation, 2) Lower Paleocene Clayton Formation, 3) Upper Paleocene Nanafalia Formation, 4) Upper Paleocene Tuscahoma Formation, 5) Middle Eocene Claibor_ne Group sediments, 6) Upper Eocene Ocala Group sediments; and 7) Oligocene sediments. An additional episode of exposure, weathering, and erosion during deposition of the Nanafalia Formation recognized in the Andersonville bauxite district (Cocker, 2003a, b), is evidenced by bauxite and kaolin clasts within the Nanafalia Formation. The complex depositional, weathering, and erosional history of the Tertiary sediments pose a number of mapping and stratigraphic identification difficulties, particularly the placement of the lower contact ofthe Altamaha Formation between mapped control points.
Exposed contacts between the Altamaha Formation and older formations indicate a complex erosional surface with significant relief present at the time of Altamaha deposition. Although the extent of post Clayton and preNanafalia erosion is unknown, exposures of the Clayton Formation residuum may only be a few feet thick.
Reconnaissance drilling and this year's mapping suggest a larger extent to the Springvale district than had been previously examined, and the earlier drilling by the U.S. Bureau of Mines inadequately defined the mineral potential of this district. Extensive coarse gravel in the Providence Formation in the Hatcher quadrangle may of economic significance because of the lack of identified hard aggregate in the Coastal Plain, proximity to a rail line that runs through the Hatcher quadrangle, and the possibility of barge transport on the Chattahoochee River only a few miles away.
Structural features observed in the map area include synclines, bedding tilted opposite to the regional trend, and multistage jointing, and faulting. Common small scale faults were noted in an earlier report on the Springvale district. Cenozoic to Pleistocene faulting and folding in and adjacent to the Southeastern Coastal Plain has been documented by previeus authors, and structural deformation noted in this report and in previous STATEMAP open file reports is consistent with and supports the previous studies.
Several occurrences of exotic, multilithic conglomerates are indicative of a high-energy environment and are lithologically inconsistent with adjacent lithologies. The ages of these sediments are uncertain but are believed to be post Upper Cretaceous Providence Formation to early Lower Paleocene Nanafalia Formation and post Eocene Claiborne Group and pre-Miocene Altamaha Formation. These may be tsunami deposits related to the impact at the KIT boundary in the Yucatan, and the late Eocene impact in Chesapeake Bay.
89

Recharge of the Claiborne aquifer occurs through the Claiborne Group sediments in the Carnegie and Doverel quadrangles, particularly on the interfluve areas underlain by the Claiborne Group sand. Permeability of the Claiborne Group sediments is adversely influenced by an increase in clay content. The mapped distribution of the chert and clay residuum found between the Altamaha Formation and the Claiborne Group marks the theoretical limit of the Upper Floridan aquifer. Recharge of the Upper Floridan aquifer in the map area is probably nonexistent, as the clay residuum indicates that the Ocala Limestone is not present.
Surface recharge of the Clayton aquifer is nonexistent in the current map area as the Clayton Formation has been eroded or it is represented only by a residuum of iron oxide and clay. Recharge may occur in the Carnegie and Doverel quadrangles but .is expected to be minimal as recharge would have to come through adjacent aquifers in the subsurface.
Recharge of the Cretaceous Providence aquifer can occur over most of the Hatcher quadrangle and much of the northern part of the Morris quadrangle.
Exposure of soft, sandy stratigraphic units such as the Claiborne Group and the Providence Formation may result in severe and rapid erosion of these sandy units. Such erosion, which is commonly related to road drainage culverts, can severely threaten the integrity of the road, as well as pose a hazard to road right-of-way maintenance crews. In addition, erosion of the sand leads to sedimentation of the larger streams and deterioration of stream habitats and water quality. Erosion gullies tend to attract illegal dumping of tires, appliances and other refuse, some of which may contain hazardous materials. As the Claiborne is an important aquifer, these materials may enter the aquifer leading to contamination down gradient.
REFERENCES CITED
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Bybell, L. M. and Gibson, T. G., 1982, The Eocene Tallahatta Formation of Alabama and Georgia: its lithostratigraphy, biostratigraphy, and bearing on the age of the Claibornian Stage: United States Geological Survey Professional Paper 1615, 20 pp.
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90

Clark, L. D., 1965, Bauxite deposits of the Springvale District, Georgia: U.S. Geological Survey Bulletin 1199-F, 24 pp.
Clarke, J. S., Faye, R. E., and Brooks, R., 1983, Hydrogeology of the Providence aquifer of southwest Georgia: Georgia Geologic Survey Hydrologic Atlas 11, 5 pl.
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Cocker, M.D., 1999a, Digital geologic map of Georgia (Version 2): Georgia Geologic Survey Documentati~n Report 99-20, 25 pp, one CD-ROM
Cocker, M.D., 1999b, Digital geologic map of the Byromville quadrangle, Georgia: Georgia Geologic Survey Documentation Report 99-03, 19 pp., plus one CD-ROM
Cocker, M.D., 1999c, Digital geologic map of the Drayton quadrangle, Georgia: Georgia Geologic Survey Documentation Report 99-04, 19 pp., plus one CD-ROM
Cocker, M.D., 1999d, Digital geologic map of the Leslie quadrangle, Georgia: Georgia Geologic Survey Documentation Report 99-05, 19 pp., plus one CD-ROM
Cocker, M.D., 2000a, Digital geologic map of the Smithville East quadrangle, Georgia: Georgia Geologic Survey Documentation Report 00-25, 21 pp., plus one CD-ROM
Cocker, M.D., 2000b, Digital geologic map of the Smithville West quadrangle, Georgia: Georgia Geologic Survey Documentation Report 00-26, 21 pp., plus one CD-ROM
Cocker, M.D., 2000c, Digital geologic map of the Bronwood quadrangle, Georgia: Georgia Geologic Survey Documentation Report 00-27, 21 pp., plus one CD-ROM
Cocker, M.D., 2000d, Digital geologic map of the Neyami quadrangle, Georgia: Georgia Geologic Survey Documentation Report 00-28, 21 pp., plus one CD-ROM
Cocker, M.D., 2001, Geologic atlas of the Bottsford, Dawson, Parrott and Shellman 7.5 minute quadrangles, Ga.: Georgia Geologic Survey Open-File Report 01-1, pp., 5 pl.
Cocker, M.D., 2002, Geologic atlas of the Americus, Lake Collins, Plains, and Preston, Georgia 7.5 minute Quadrangles, Georgia: Georgia Geologic Survey Open File Report 02-1, 74 pp., 5 plates. (scale@ 1:24000).
Cocker, M.D., 2003a, Geologic atlas of the Andersonville, Methvins and Pennington 7.5 minute quadrangles, Georgia: Georgia Geologic Survey Open File Report 03-1, 83 pp., 4 plates. (scale@ 1:24000).
Cocker, M.D., 2003b, Geologic atlas of the Americus Area, Georgia: Georgia Geologic Survey Open File Report 03-2, 21 pp., 1 plate. (scale@ 1:100000).
Cocker, M.D., 2004a, Geologic atlas of the Benevolence, Lumpkin and Richland 7.5 minute quadrangles, Georgia: Georgia Geologic Survey Open File Report 04-1, 87 pp., 4 plates. (scale@ 1:24000).
Cocker, M.D., 2004b, The relationship of unconformities to the genesis, alteration, and preservation of the bauxite and high-alumina kaolin deposits in the Andersonville District, Georgia (abs): 40th Annual Forum on the Geology of the Industrial Minerals, Bloomington, Indiana.
Cocker, M.D., 2005a, Digital geologic mapping of aquifer recharge zones in the Upper Coastal Plain of Georgia: Geol. Soc. America Abstracts with Programs, v. 37, no. 2, p. 33.
Cocker, M.D., 2005b, Geologic atlas of the County Line, Lumpkin SW, Sanford, and Twin Springs 7.5 minute
91

quadrangles, Georgia: Georgia Geologic Survey Open File Report 05-1, 59 pp., 5 plates. (scale@ 1:24000).
Cocker, M.D., 2006a, Derivative digital geologic maps useful for assessment of geological hazards in the Upper Coastal Plain of Georgia: Geological Society of America Abstracts with Programs, v. 38, no. 2.
Cocker, M.D., 2006b, Detailed quadrangle mapping aids identifying kaolin - bauxite mineral potential in Paleocene age Upper Coastal Plain sediments of southwestern Georgia: in Reid, J.F. (ed.), 42th Annual Forum on the Geology of the Industrial Minerals, Asheville, North Carolina: North Carolina Geological Survey, 1 CD.
Cocker, M.D., 2006c, Geologic atlas of the Brooksville, Cuthbert, Georgetown, and Martins Crossroads, Georgia 7.5 minute quadrangles: Georgia Geologic Survey Open File Report 05-1, 79 pp., 5 plates. (scale@ 1:24000).
Cocker, M.D., 2007a, Possible impact-related sediments in the Upper Coastal Plain of Southwestern Georgia: in King, D.T., Jr., and Ormo, J., Marine impact craters on Earth: Field investigation of the Wetumpka impact structure, a well-preserved marine impact crater, and the K-T boundary in the Alabama Gulf Coastal Plain: Wetumpka, Alabama, Wetumpka Field Forum 2007 Guidebook and Abstracts, 119 pp.
Cocker, M.D., 2007b, Geologic controls on erosion, sedimentation of streams, and potential for groundwater contamination in southwestern Georgia: in Rasmussen, T., Carroll, G.D., Georgakakos, A. eds., Proceedings of the 2007 Georgia Water Resources Conference; held March 27-29, 2007, at the University of Georgia, 4 pp, 1 CD-ROM.
Cocker, M.D., 2007c, Cenozoic and younger tectonic activity in Southwestern Georgia: Geological Society of America Abstracts with Programs, v. 39, n.o. 2, p. 89..
Cocker, M.D., 2007d, Defining the mineral potential of Upper Coastal Plain sediments in Southwestern Georgia through detailed quadrangle mapping: Geological Society of America Abstracts with Programs, v. 39, no. 2, p. 100.
Cocker, M.D., 2007e, The relationship of unconformities to the genesis, alteration, and preservation of the bauxite and high-alumina kaolin deposits in the Andersonville District, Georgia: in Shaffer, N.R. and DeChurch, D.A., eds., Proceedings of the 40th Forum on the Geology of Industrial Minerals, Bloomington, Indiana: Indiana Geological Survey, p. 30-37.
Cocker, M.D., 2007f, Possible impact-related sediments in the Upper Coastal Plain. of Southwestern Georgia: in King, D.T., Jr., and Ormo, J., Marine impact craters on Earth: Field investigation of the Wetumpka impact structure, a well-preserved marine impact crater, and the K-T boundary in the Alabama Gulf Coastal Plain: Wetumpka, Alabama, Wetumpka Field Forum 2007 Guidebook and Abstracts, 119 pp.
Cocker, M.D. and Costello, J.O., 2003, Geology of the knericus Area, Georgia: Georgia Geological Society Guidebooks, Volume 23, Number 1, 64 pp.
Cofer, H. E., Jr. and Fredericksen, N. 0., 1982, Paleoenvironment and age of the kaolin deposits in the Andersonville, Georgia district: in Arden, D. D., Beck, B. F., and Morrow, E., eds., Proceedings: Second Symposium on the Geology of the Southern Coastal Plain: Georgia Geologic Survey Information Circular 53, p. 24-37.
Cofer, H. E., Jr. and Manker, J.P., 1983, Geology and resources of the Andersonville, Georgia kaolin and bauxite district: United States Geological Survey Open File Report 83-580, 95 pp., 1 pl.
Cofer, H. E., Jr., Wright, N. A., and Carey, M. A., 1976, Preliminary report on the kaolin and bauxite deposits of the Andersonville district, Georgia: United States Geological Survey Open File Report 76-682, 22 pp.
Cramer, H. R. and Arden, D. D., 1980, Subsurface Cretaceous and Paleocene geology of the Coastal Plain of Georgia: Georgia Geologic Survey Open File Report 80-8, 184 pp.
92

Daniels, D.L., 2001, Georgia Aeromagnetic Compilation: United States Geological Survey Open File Report 01106, http://pubs.usgs.gov/openfile/ofD 1-106
Eargle, D. H., 1955, Stratigraphy ofthe outcropping Cretaceous rocks of Georgia: United States Geological Survey Bulletin 1014, 101 pp.
Fallaw, W.C. and Price, V., 1992, Outline of stratigraphy at the Savannah River Site: in Fallaw, W.C. and Price, V., eds., Geological Investigations of the Central Savannah River Area, South Carolina and Georgia: Carolina Geological Society Field Trip Guidebook, p. CGS-92-II-1 - CGS-92-II-25.
Frey, R.W. and Pemberton, S.G., 1984, Trace fossil facies models: in Walker, R.G., ed., Facies Models, Second Edition, Geoscience Canada, Reprint Series 1: Geological Association of Canada, p. 189-207.
Fritz, W. J., ed., 1989, Excursions in Georgia Geology: Georgia Geological Society Guidebooks, vol. 9, #1, 264 pp.
Furcron, A. S., 1956, Iron ores of the Clayton Formation in Stewart and Quitman Counties, Georgia: Georgia Mineral Newsletter, vol. IX, p. 116-123.
Georgia Geologic Survey, 1976, Geologic map of Georgia: Georgia Geological Survey, Atlanta, Georgia, 1:500,000 scale.
Gibson, T. G., 1982, Paleocene to Middle Eocene depositional cycles in eastern Alabama and western Georgia Coastal Plain: in Arden, D. D., Beck, B. F., and Morrow, E., eds., Proceedings: Second Symposium on the Geology of the Southern Coastal Plain: Georgia Geologic Survey Information Circular 53, p. 53-63.
Gohn, G. S., Bybell, L. M., Christopher, R. A., Owens, J. P., and Smith, C. C., 1982, A stratigraphic framework for Cretaceous and Paleocene margins along the South Carolina and Georgia Coastal sediments: in Arden, D. D., Beck, B. F., and Morrow, E., eds., Proceedings: Second Symposium on the Geology of the Southern Coastal Plain: Georgia Geologic Survey Information Circular 53, p. 64-74.
Gorday, L. L., Lineback, J. A., Long, A. F., and McLemore, W. H., 1997, A digital model approach to water-supply management of the Clairborne, Clayton, and Providence aquifers in southwestern Georgia: Georgia Geologic Survey Bulletin 118; 31 pp., 2 supplements.
Harris, R. S., Roden, M.F., Schroeder, P.A., Holland, S.M., Duncan, M.S., and Albin, E.F., 2004, Upper Eocene impact horizon in east-central Georgia: Geology, v. 32, no. 8, p. 717-720.
Harris, W. B. and Fullagar, P.D., 1982, Rb-Sr isochron, Twiggs Clay Member of the Dry Branch Formation, Houston County, Georgia: Carolina Geological Society Field Trip Guidebook 1982, p. 47-55.
Herrick, S.M., 1961, Well logs of the Coastal Plain of Georgia: Georgia Geologic Survey Bulletin 70, 462 pp.
Herrick, S.M. and Vorhis, R. C., 1963, Subsurface geology of the Georgia Coastal Plain: Georgia Geologic Survey Information Circular 25,78 pp.
Hetrick, J. H., 1990, Geologic atlas of the Fort Valley area: Georgia Geologic Survey Geologic Atlas 7, 2 pl.
Hetrick, J. H., 1992, A geologic atlas of the Wrens-Augusta area: Georgia Geologic Survey Geologic Atlas 8, 3 pl.
Hetrick, J. H., 1996, Geologic atlas of the Butler area: Georgia Geologic Survey Geologic Atlas 9, 8 pp., 1 pl.
Hetrick, J. H. and Friddell, M. S., 1990, A geologic atlas of the central Georgia Kaolin District: Georgia Geologic Survey Geologic Atlas 6, 4 pl.
Huddlestun, P. F., Marsalis, W. E., and Pickering, S. M., Jr., 1974, Tertiary stratigraphy of the central Georgia
Coastal Plain: Georgia Geologic Survey Guidebook 12, Part 2, 35 pp. Huddlestun, P. F., 1993, A revision of the
93

lithostratigraphic units of the Coastal Plain of Georgia: The Oligocene: Georgia Geologic Survey Bulletin 105, 152 pp.

Huddlestun, P. F. and Hetrick, J. H., 1979, The stratigraphy ofthe Barnwell Group of Georgia: Georgia Geological Society, 14th field trip guidebook: Georgia Geologic Survey Guidebook 18, 89 pp.

Huddlestun, P. F. and Hetrick, J. H., 1985, Upper Eocene stratigraphy of central and eastern Georgia: Georgia Geologic Survey Bulletin 95, 78 pp.

Huddlestun, P. F. and Hetrick, J. H., 1991, The stratigraphic framework of the Fort Valley Plateau and the central Georgia kaolin district: Guidebook for the 26th Annual Field Trip, Georgia

Huddlestun, P. F., 1985, An examination of the Altamaha Formation near Oak Park, Emanuel County, Georgia: Georgia Geological Society Guidebooks Volume 5, Number 1, p. 1-19.

Huddestun, P. F., 1988, A revision of the lithostratigraphic units of the Coastal Plain of Georgia: The Miocene through Holocene: Georgia Geologic Survey Bulletin 104, 162 pp.

Huddlestun, P. F., 1992a, The Paleogene of the northeastern Gulf of Mexico Coastal Plain: in Zullo, V. A., Harris, W. B., Price, V., eds., Savannah River Region: Transition Between the Gulf and Atlantic Coastal Plains: Proceedings of the Second Bald Head Island Conference on Coastal Plains Geology, University of North Carolina at Wilmington and U. S. DOE, p. 23-24.

Huddlestun, P., 1992b, Upper Claibornian coastal marine sands of eastern Georgia and the Savannah River Area: in Fallaw, W.C. and Price, V., eds., Geological Investigations of the Central Savannah River Area, South Carolina and Georgia: Carolina Geological Society Field Trip Guidebook, p. CGS-92-XII-1 - CGS-92-XII-6. Geological Society, vol. 11, no. 1, 119 pp.

Huddlestun, P. F., Marsalis, W. E., and Pickering, S. M., Jr., 1974, Tertiary stratigraphy of the central Georgia Coastal Plain: Georgia Geologic Survey Guidebook 12, Part 2, 35 pp. Huddlestun, P. F., 1993, A revision of the lithostratigraphic units of the Coastal Plain of Georgia: The Oligocene: Georgia Geologic Survey Bulletin 105, 152 pp.

Huddlestun, P. F. and Hetrick, J. H., 1979, The stratigraphy of the Barnwell Group of Georgia: Georgia Geological Society, 14th field trip guidebook: Georgia Geologic Survey Guidebook 18, 89 pp.

Huddlestun, P. F. and Hetrick, J. H., 1985, Upper Eocene stratigraphy of central and eastern Georgia: Georgia

Geologic Survey Bulletin 95, 78 pp.



Huddlestun, P. F. and Hetrick, J. H., 1991, The stratigraphic framework of the Fort Valley Plateau and the central Georgia kaolin district: Guidebook for the 26th Annual Field Trip, Georgia

Johnston, R. H. and Miller, J. A., 1988, Region 24, Southeastern United States: in Back, W., Rosenhein, J. S., and Seaber, P. R., eds., Hydrogeology, Geological Society of America, The Geology of North America, Hydrogeology, vol. 0-2, p. 229-236.

Kirkpatrick, S.R., 1959, The geology of a portion of Stewart County, Georgia: MS Thesis, Emory University, 79 pp.

Kirkpatrick, S.R., 1963, Geology of the Lumpkin SW quadrangle, Stewart County, Georgia: The Compass, v. 41, no. 1, p. 40- 51.

Long, A. F., 1989, Hydrogeology of the Clayton and Claiborne aquifer systems: Georgia Geologic Survey Hydrologic Atlas 19, 6 pl.

Luckett, M.A., 1979, Cretaceous and Lower Tertiary stratigraphy along the Flint River, Georgia: unpublished M. S. Thesis, University of Georgia, 51 pp.

94

Marsalis, W. E. and Friddell, M.S., 1975, A guide to selected Upper Cretaceous and Lower Tertiary outcrops in the lower Chattahoochee River valley of Georgia: Georgia Geologic Survey Guidebook 15, 87 pp.
McFadden, S. S. and Perriello, P. D., 1983, Hydrogeology of the Clayton and Clairborne aquifers in southwestern Georgia: Georgia Geologic Survey Information Circular 55, 59 pp.
Mitchell, G. D., 1981, Hydrogeologic data of the Dougherty Plain and adjacent areas, southwest Georgia: Georgia Geologic Survey Information Circular 58, 124 pp., 3 pl.
Nystrom, Jr., P.G. and Willoughby, R.H., 1982, Cretaceous, Tertiary,' and Pleistocene (?) stratigraphy of Hollow Creek and Graniteville quadrangles, Aiken County, South Carolina: in Nystrom, Jr., P.G. and Willoughby, R.H., eds., Geological investigations related to the stratigraphy in the Kaolin Mining District, Aiken County, South Carolina: Carolina Geological S'ociety Field Trip Guidebook, p. 80-109.
Owen, V., 1956, Stratigraphy and lithology of southern Webster County, Georgia: unpublished M.S. thesis, Emory University, 82 pp., plus map, cross-section and stratigraphic column.
Prowell, D.C., 1983, Index of Cretaceous and Cenozoic faults in the eastern United States: U. S. Geological Survey Miscellaneous Field Studies Map MF 1551.
Prowell, D.C., 1988, Cretaceous and Cenozoic tectonism on the Atlantic coastal margin: in Sheridan, R.E., ed., The Atlantic Continental Margin, U.S.: The Geology of North America, v. 1-2: The Geological Society of America, Boulder, CO, p. 557-564.
Reinhardt, J., 1982, Lithofacies and depositional cycles in Upper Cretaceous rocks, central Georgia to eastern Alabama; in Arden, D. D., Beck, B. F., and Morrow, E., eds., Proceedings: Second Symposium on the Geology of the Southern Coastal Plain: Georgia Geologic Survey Information Circular 53, p. 89-96.
Reinhardt, J., 1986, Stratigraphy and sedimentology of continental, nearshore, and marine Cretaceous sediments of the eastern Gulf Coastal Plain: Society of Economic Paleontologists and Mineralogists Field Trip #3, AAPG Annual Meeting, Atlanta, Georgia: Georgia Geologic Survey, 99 pp.
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Reinhardt, J., Prowell, D.C., Christopher, R. A., 1984, Evidence for Cenozoic tectonism in the southwest Georgia Piedmont: Geological Society of America Bulletin, v. 95, p. 1176-1187.
Sever, C.W., 1966, Reconnaissance of the Ground Water and Geology of Thomas County, Georgia: Georgia Geologic Survey IC 34, 14 pp.
Smith, R. W., 1929, Sedimentary kaolins of the Coastal Plain of Georgia: Georgia Geologic Survey Bulletin 44,482 pp.
Toulmin, L. D. and LaMoreaux, P. E., 1963, Stratigraphy along the Chattahoochee River, connecting link between . Atlantic and Gulf Coastal Plains: American Association of Petroleum Geologists Bulletin, volume 47, #3, p. 385-404.
Toulmin, L. D., LaMoreaux, P. E., Newton, J.G., 1964, Profile showing geology along the Chattahoochee River: The Geological Survey ofAlabama SM 28, 1 plate.
Zapp, A. D. and Clark, L. D., 1965, Bauxite in areas adjacent to and between the Springvale and Andersonville
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Districts Georgia: United States Geological Survey Bulletin 1199-H, p. H1- H10,1 pl. Zullo, V.A., Willoughby, R.H., Nystrom, P.G., 1982, A late Oligocene or early Miocene age for the Dry Branch
Fonnation and Tobacco Road Sand in Aiken County, South Carolina: Carolina Geological Society Field Trip Guidebook 1982, p. 34-45.
96

UNITED STATES DEPARTMENT OF THE INTERIOR
GEOLOGICAL SURVEY

Georgia Geologic Mapping Program Open-File Report 07-1

Plate 1

EUFAULA SOUTH QUADRANGLE
ALABAMA-GEORGIA 7.5 MINUTE SERIES (TOPOGRAPHIC)
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Locatwn Map of the Eufmula South 7.5 mmute quadrangle
Explanation
Detailed descriptions of rock units ioclmded in text of Open File Report 07-1
Map Units
C J Water
C J Qal -Quarternary All uvmm -poorly sort<ed s11t, sand and gravel C J Kr- Upper Cretaceous Ripley Formallom- massrve, btotwbatcd, fine lo medmm, mJcaceous, glaucomttc,
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Mapped, edtt~d. and published by the Geological Survey
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Geologic Map of the Eufaula South Quadrangle, Georgia

~ Contact (lot;alcd approximately)
GcoloJ:,>y by Mark D Cocker Dgtized and dtg1ta!ly complied by Mark D. Cocker Map projec1:!on, Albers Corne Equal Area NMD27 August, 2007 Supp01ted by the US GeologiCal Survey, Nmtional Coopcra1:!vc Geolog1c Mappmg Program, under nsststnncc A11ard PA.~o,'Tcement #06HQAG0044

UNITED STATES DEPART MENT OF THE JNTERJOR
GEOLOGICAL SURVEY
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WA.f..TE.' R F GEORGE RESERVOIR

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Georgia Geologic Mapping Program Open-File Report 07-1
Plate 2

Locatwn Map of the Hatteher 7 5 minute quadrangle

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Mapped , edtt ed, and publts.h ed Dy th.P. Geological Survey
CC~ntw l by USGS. USC & GS, and G~o rgw C eo d et r ~ Sur vey
Topography by pho togrammi't nc m oe-tl1od~ from il!l" ~ l ph otoflraph s taken 1965 FeloJ checked 196 7
Po'ycorHc pro tectron 19 27 North 1\men.:: an d<ltlJm 10,()0/). fool g rid Oased on Georgra ~oo rdtnate s ~stcm. "'~ 5 t zone
lOOO.rne ter Unt~ersal Tran5\lerse Me.r ~;ato r gno trc k~ , 2o ne 16,
s f1o wn rn l:!ll!e
Ftne red rh sh~d Ime~ tndtcate seleLted fen~;e and t el~ lro1cs ..,~,r~ !l ei'\Ha!ly ~ISI(l l ; on a~na l photner 11phs. Tht s rn torm~licn is LOn ~ hec ~ sd

~I

I!Tfot G~tD Al\tD ,%7 MAG.,.fTI C: NOP. TH DC!;U NMION H O::E:Io/ TEI< Cf S Hl El

l

,

0

~-'-l-- ...,....:{"~~""'"'""'"""'~~

CO N f O UR INT ER VAl 10 F En

DAi' llM IS MEli N SEll 1 EVEL

J ~ J( o) M ~i! R
=

f t-11<1 MAP (:() r.:P LIL:-i WII H NMI G N4J t'-1~1"' t.I'CU RACY STANDA RDS FOR SALE BY U.S. GEOLOGICAL SURVEY. WASHINGTON . D C. 2:0.'<:42 A FOLDtfl IJt:SCI<li:IINFl rrtFOGAIIPHI C M APS .'I.Nll <>'YM OOL S I'S .JI.YJio llitBL E ON REQUEST

ROA D ClASSIFICATION

Prirnary h1gh11'ay. a\I weather,
ha rd surface .:. . __ _ _ __

Ltght-duty road , ~II we~ther, rrnpro~ed 'l.u rface -~~~~

Ser;ondary l'ughwaJ', all l'llli!ttll!r, Ummproved road , fatr or d.ry

h.ud surface _ __ _ --~- weather .

- -~=~ "'" "'~~

0 IJ S Rc~te

Q State Route

HATCHER, GA .
N3145- W8S00/7 5
1967

Geologic Map of the Hatcher Quadrangle, Georgia

r

Explanation
Detailed descriptions or rock units jndutded in text of Open File Report 07-1
Map Units

C J Water

C J Qat- Quartemary Alluvmm- poorly ~orted stll, sand an d gm"cl

C J Tn- M1ocene Altamaha Formatron - mass lt\IC flr[~tllaccous sandstone
C J Tnf- Upper Paleocene Nnnafalm Formal~<on- cross-bedde~ fine lo vel)' coarse, micaceous quartz sand<>tone_ kaolin, and bauxile

Tel - Lower Paleocene Clayton Fonnatrom- mterbcddcd, mu.:accom: silty clay, calc<ircous sandstone, and bioc lastiC !J mestone

Kp - Upper Cretaceous Providence Fonnmtlo1J- cross-bedded, loca lly m cnceous, fi ne lo coarse sand

wttb mtcrbcddcd, mas~vc to Lh1nly boedded, sandy clay lenses

.

I

IKr- Upper Cretaceous Ripley Formation -- mas1tve, bioturbated, fine to medium, micaceous, glnucomtlc, calcareous quarlz sand g1radm~ upward to mnssr\o e fine sand to stlty clay

IY'VI Ct oss Section

~ Corc Holc
~ Contact (located approxunalely)

GcolO!,'Y by fV[ark D Cocker OtgJtlzcd and dlgLI:a lly comptled by Mark D Cocker Map proJectton, Albers Come Equal Area NAD27 August 2007 Supported by the U.S Geological Survey, National Cooperatne Geologtc Mappmg Progmm, under assistance Award Agreement #06HQAG0044

Cross-Section A -A' Hatcher Quadrangle

~

Explanation
Allmrium (Holocene and Pleistocene)- Variably micaceous, poorly smt ed, ftne-to coarse-grained sedimenl and variable amounts of organic matter deposited in channels, flood plains, and marshes

~ ~

Nanafalia Formation (Upper Paleocene) - Cross-bedded to massive, light greenish-gray to yellowish-brown to white, highly micaceous, kaolinltic, fine- to very coarse-brrained, quartz sandstone_ May contain abundant, rounded or subrounded kaolin clasts and local ly contains large lenses or layers of economic high-alumina kaolin and bauxite deposits.
Providence Formation (Upper Cretaceous)- Cross-bedded, locally micaceous, fine to coarse sand with interbedded, masslvc to thinly bedded, sandy clay lenses.

~

Ripley Formation (lJpper Cretaceous)- Massive, bioturbated, fine- to medium-grained, micaceous, glauconitic, calcareous quartz sand grading upward to massive fine sand to silty day_

Horizontal Scale: 1" = 2000'

NW

110"-----<

Vertical Scale: I'= I00'

A

-~50~0~---------------------------------------------------------------------------T-n-f---------------u"~~"0>'-

400

g

~

~ u
.5>

-~""

n. --/- -.-._ ~ Qal~ Qal /"\ Qal

f /-

\ 1/ -

~\

Tnf

Tnf

Qal

300

\

<C}

Qal

Tnf
---------- ------------- -------- --------------------- ----- ----------------- - ------------ ------

I

--~ -

Kp Kp
200

------- - ---------------- --- -- ----- -- ------ ------ - -------- - - - ------------------------------------------------ - ---------------------------------------------------
Kr

------------------------------- - -- --- - - ----- - - - ------- - ---------- - - ------ - ------------- -- -------- --- - -- -- - -- -- - -- - -
Kr

SE

A'

u-"""

500

"

@

u 400

300

or

&
' I

200

Kr

UNlTED STATES DEPARTMENT OF THE JNTERlOR
GEOLOGJCAL SURVEY

STATE OF GEORGIA
DEPARTMENT OF MINES, MINING, AND GEOLOGY DIVISION OF CONSERVATION

Georgia Geologic Mapping Program Open-File Report 07-1
Plate 3

LocatJon Map of the Morns 7 5 Minute quadrangle

Mapped ed ttG d, and pu t.!rshed by th0 GeologJca l Survey
Con tro l by USGS USC&GS, anci G~org,.., r;eod~trc Sll rvey
Topogr~phy b1 prtotoer.amme lnc methods from aenal !)holograph s ta ken 1972 FnJd checked 19 7 3
Protedron <md 10,000 loo t gr1d lr t:k~ Gc\.lrgra coord r n~to> ~,'!'i t em "'"~t z01. (trom sverse MPtC.llor) 1000 mNer Um"crs~l Trii~Sverse Merc.:otm gnd trcks zor>e 16, shown rn lll Lte 1927 NorUr Amcn t:ill'l d atum
Fme red dash ed lr nes rndrcate select~ lent.e ~nrl lrl'ld l 1r1e~ 'f>herii r,cMr,!,y v ri.Jic -on ..l'r ra' photo.gr ~p h-;. Th~ 111for matro n r!; unr IJed~:U

UTI GRm AH ll \9"73 1>1/.r:NETIC WORTH DECLINATON ~T HI<ICR Of SKEH

SCAI E: l 24 000
CO N T OU~ l"ilERVt,l 10 FEU
Nl'l iONIL t>t:ODET IC VR1rC,\L 0 \IUM OF 1929
THIS MAC' C0~1PLUOS WH H NATION.<.L MAP ~C ClJRACi -;TANDAIWS FDR SALE 6 '( U 5 G[OLOCICAL SURVE'f , Rt-::;TON W~ GINIA 22092 A roWER DtSCRl6 lNG TOI'OGRA. PfiiC MI\PS AN O SYMBOLS IS AVAILI\iJLE ON ktQUESl

"'' ROAD CU\SSIFI C!I.TION

Pnrn ar,. hrghwa~ . ha'd ~urface

L1ght-duty road hard Of
rmproved surfar.e - -- - -

Secondary hrghway

l rard su!ace _ ~-~ Ur11m~roved road --~~ - -- -~

Cr ~ 1 1nters~le Route f U S Route

Stale Rout'"-

MORRIS, GA
N-3 14 5 -W8452 5/7 5
1973

Geologic Map of the Morris Quadrangle, Georgia

Explanation
Detailed descriptions of rock units includted in text of Open File Report 07-1
Map Units

C J \Vuler

C J Qal -Quarternary Alluvmm - poorly so1rted silt, sand and gra\c]

C J Ta- M10cene Altamaha I'ormation- matssJve argtllaceous sandstone

C J Tcb - Lower to M1ddlc Eocene Clmbormc Group- mass1ve to cross-bedded, fine to coarse sand and sandstone

C J Ttu - Upper Paleocene Tuscahoma Fornnat10n- nonfossthfcrous mter-lammatcd cl ay, srlty clay, and fine quartzose sand

I

I Tnf Upper Paleocene N anafnha Formation- cross-bedded, fine to \CI)' course, micaceous quartz snndstone, kaohn, and bauXIte

lei- Lov~-er Paleocene Clayton Fonnat1ron- irlc rbcdded, mrcaccom; s1lty clay, calcareous sandstone, and broclast1c limestone

Kp- Upper Cretaceous Prov1dcnce Fomnatwn -cross-bedded, locally rmcaceous, fine to coarse sand w1th mtcrbed ded , massne to tlhmly bedded, sandy clay lenses

Kr - Upper Cretaceous Ripley Fonuat10m - massrve , bwturbated, fine to medmm, m1caceous, glaucomUc, calcareous quartz sand gradmg upward to maSSIVe fine sand to Silly clay

Cross Scclwn

l/SVj Contact (located approxtmateh)

Geology bj Mark D Cocker D1gt7.ed nod d1g:ttally comp1lcd by Mnrk D Cocker Mnp proJection, Albers Come Equal Area NAD27 AugusL 2007 Supported by the US Geolog1cal Survey, National Cooperative Geolog 1c lvl.appmg Program Lmder assistance AwardAgrcemcnl #06HQAG0044

Cross-Section A - A' Morris Quadrangle

Explanation

~

Alhwium (Holocene and Pleistocene)- Variably micaceous, poorly sorted, fme- to coarse-grained sediment and variable amounts of organic matter deposited in charu1els, flood plains, and marshes.

[ Too I

Claiborne Group (Lower to Middle Eocene)- Ma:-;sivc to finely laminated, locally cross-bedded, white to light tan to brick red, locally kaolinitic, fine- to coarse-grained sand and poorly indurated sandstone. Unconformably overlies the Tuscahoma and Nanafalia Fom1ations. Highly susceptible to rapid erosion_

~

Tuscahoma Formation (Upper Paleocene to Lower Eocene)- Non-fossiliferous, gray, red or purple, interlaminated clay, silty day, and fine quartzose sand . May locally be overlain by the Bashai Member of the Hachetigbee Fonnation consisting of light to dark greenish-gray, dominantly massive, well-sorted, very fine- to fin e-grained
qua1tz and glauconite sand.

~

Nanafalia Formation (Upper Paleocene) -Cross-bedded to massive, li.gbt greenish-gray to yellO\vis.h brown to white, highly micaceous, kaolinitic, fine- to ve ry coarse-grained, quartz sands lone. May contain abundant, rounded or subrounded kaolin clasts and locally contains. large lenses or layers of economic high-alumina kaolin and bauxite
deposits.

~

-Providence-Formation (Upper Cretaceous)- Cross-bedded, locally micaceous, fine tocoarse sand with interbedded;massivc to thinly bedded, sandy clay lenses.

NW
A
500

116 - - -

- - - - - - --

Horizontal Scale: l" = 2000' Vertical Scale: 1' = 100'

- - - - - - - - - - - - - - - -- -

--

---

400

- - - - - - ----

1j

1

300

~
u

"- . ~
" I \ ~a\0::

----';';;:-- - --

- --

-----

= a

&

Qal

~ Qal

~

I

/ '

-'--- -- - -------

200 -- -- - - ,\ _

,_I

I

.--- - - - - - - - -- ..

Tnf

/-

~--\

- A 1
-/.

/\./ -

' Tnf
/ /
Qal

--

K~

Kp

SE
~ 500

Tcb...._

Tcb
____...,.._____ __
- - - ---- - - - - J---1. -+------ -------------~-.--

Tcb 400
'----~----- --~l--

-

----------------

Ttu
--- ------- -------__- --___ - ----=----~ ....

300
---------

Tnf
--"- '- -~-- =~---

200

Kp

UNITED STATES DEPARTMENT OF THE INTERIOR
GElOLOGIC.AL SURVEY
0 '(
. ~ 91'~
Itu 1
,r
. I
.''I
lj [
42'30"

STATEl OF GEORGIA
DEPARTMENT OF NA T URAL "RESOURCES
EARTH ANO WATER DiVISION
't-O.:. 'T IV S E"
1IJ7 IC I.JT!-IBERTJ,

Georgia Geologic Mapping Program Open-File Report 07-1
Plate 4
CARNEGIE QUADRANGLE
GEORGIA-RANDOLPH CO. 7.5 MINUTE SERJES (TOPOGR APHIC)

Location Map oftlne Carnegie 7.5 minute quadrangle

/

\ .._!

r

I,, j

\.'

/

ll 0

,1 ~

I
"

\ 4()'
r

. ']~
I
\',I' ,I I"

I I'

Explanation

Detailed descriptions of rock units induded in text of Open File Report 07-1
Map Units

C J \Vater

C J Qal- Quatcrnmy Alluv ium - poorl:y sorted si lt, sand and .S'Hivel

C J Ta- Miocene Altamaha Formationt- massive argi llaceous sandstone

C J Tsr- Tertiary Sediments and Rcsidtuum - massive waxy clay cmd locally abundant chert

C J Tcb - Lower to lvliddle Eocene Clatiborne Group- massive to cross-bedded, fine 1o coarse sand and sandstone

C J Ttu- Upper Paleocene Tuscahoma Formation - nonfossiliferous, inter-laminated clay, s ilty clay, and fme quartwse sand

I

I Tnf - Upper Paleocene Nanafalia Formation- cross-tcdded, fine to very coarse, micaceous quartz sandstone, kaolin, and bauxitCe

IYV"I Cross Section

~ Contact (located approximately)

TH IS MAP C0M PUS W ITH NAT IONAl.. M AP AGClHlA CY STA fWAR OS
fO!'l SI\LE BY U.S . GEOLOGICAL SURVEY, RESTON, \ii RGtNIA 22092 A I'OLD~Cn OESGRI!l lf'I G TO t'OGIU,PHIC MII.P$ AND SYMfi'O LS IS JIV/IIl.A8L( ON R~Q li !OSf

CARNEG!E, GA.
l'i 313 "! .5-WS44 5/7.5
191'3

Geologic Map of the Carnegie Quadrangle, Georgia

Geology by Mark D. Cocker Digiti zed and digitally compiled by r-v"Aark D. Cocker Map projection, Albers Conic Equal A\rea NAD27 August, 2007
Supported by the U.S. Geological Sumey, National Cooperative Geologic
Mapping Program, tmder assislancc ft\.ward Agreement #06HQAG0044

Cross-Section A - A' Carnegie Quadrangle

~

Ex pI anati on
Alluvium (Holocene and Pleistoce ne)- Variably micaceous, poorly sorted, fine- to coarse-grained sediment and variable amounts of organic matter deposited in channels, flood plains, and marshes.

IT]

A ltamaha Formation (Miocene)- Massive, brick red, argillauoous, nwderately indurated, line-grained to gritty
sandstone containing variable amounts of small , rounded, generally black, "ironstone" pebbles _ A basal
conglomermc tbat may contain chert residuum, .iron-oxide cemented sandstone or iron-oxide crusts is usually present. Unconformably overIies all other stratigraphic units at least to the Upper Cretaceous Providence Formation.
Fonns a caprock that prote{'.ts underlying softer, more easily eroded sediments and is the source Cor the best agricultural soils in thi~ part of Georgia May be extensively mottled in upper pans of exposures due to the dovmward migration of water and day

~

Tertiary Sediments and Residu um (Eocene to Oligocene?)- Includes bmwn W orange, mottled, sticky clay and
massive, \Vhitish, locally fossiliferous chert fragments_ Clay may be massive or exhibit distorted, tine layering. Clay and chert fragments are commonly intennixed. This residuum may be the weat hered equivalents of Rocene to Oligocene earbonate rocks. This unit is highly discontinuous in the map area_

~

Claiborne Group (Lower to Middle Eocene) - Ma~sive to finely laminated, locally cross-bedded, while to light tan to
brick red, locally kaolinitic., fine- to coarse-grained sand and poorly indurated ~andslone_ Unconformably overlies
the Tuscahoma and NanafilJia Formations. Highly susceptible to rapid erosion.

~

Tuscahoma !'ormation (Upper Paleocene to Lower E-ocene)- Non-fossiliferous, gray, reJ or purple, interlaminated
clay, silty clay; and fine quartzose sand_ May locally he overlain by the Ba.'!hai Member of the Hacheligbee
Formation consisting ofl ight to dark greeni~h-gray, dominantly massive, well-sorted, very fine- to !lne-graincd
quartz and glauconite sand.

--~

- cr;;r:J

--N~nafalia-li'ol:mation.(Upper ltaleuceoe) - Cross-bedded to.massi-ve;-li.ghLgreenish"gray t o yellowi-sh brown- !.o-white,

highly micaceous, kaolin itic, fine- to very coarse-grained, quartz sandstone. May contain abundant, rounded or

subrounded kaolin clasts and locally contains large lenses or layers of economic high-alumina kaolin and bauxite depo~its. lin confonnably overlies Lhe Clayton Formation .



Clayton Forma lion (Lower Paleoce ne) - l\.fainly a residuum of red, buff lo dar-k brown, \vhite to light grny and black
clay, white chert, and red to black iron oxide masses_ Jn the subsurface, it consists of yel low to buft~brown,
interbedded, micaceous silty clay, calcareous sandstone, Hnd light gray biocla~tic limestone

NW

A

116"'- --o 500

11
u ~

l

400

7 __ ___ At--! "--,"
'/_:___,_Ico Teo

Teb - ~~a! _ _ _ __

Ttn

-----------

Tiif

- - - - -

Horizontal Scale: 1" = 2000' Vertical Scale: I'= 100'

-- --------

Ta --- --- --- ---- - --

" 0
u ~
"u"
------ -

~ u
0
--"j0

200
Ttu
Tnf

Tcb

SE
A'
500
400
300
I 2oo

UNITED STATES DEPARTMENT OF THE INTERlOR
GEOLOGICAL SURVEY
.84" 3i' ':.i0 " 3 1 ~ 45'

Georgia Geologic Mapping Program Open-File Report 07-1
Plate 5

Ta
Location Map of the Doverei 7,5 minute quadrangle

M<! ppe1. edited. and p~b! i s.h ed hy the Geolog1cal SuNey
Co!"ltr oi by USGS ~r,IJ U~C& GS
Topogr Jp hv ~ p~ut ogra m:ne t r Jc method !:. frorn .!l ~r, a l
pnocoe raphs ta\(en EJ7L F1d(i ch!! cked 1973
ProteG i io n rond 10 ,000-foo t g r~d l 1clt ~ G rtoog ill CQ<)nj matc sr~re 1n . w.r.:l Lonol;' (tra nf.lf:!l1'.1'1 MertMori lOOQ -rn e!er U n!!!: rs~/ T r !!1~1 flr~ ,; ~-111!l Cato r grtd ti r;ks , LO ne 1 6. .s. ho"'n m tllue. 19 ;'>7 N v t1 Arnerl (~ l~ aatu m
F1:--oe rml dcsnarJ li nes ,; ~ di o::at'"- ">e l ~d~U fence ~n(J f l t.ld l i nes ..,h~re g~ n er ;a hy v1si t:>l e on &~! ria l Dho wgr<i pt\;;. 1 r,.,:;. in t orrn<'l li O:J is ur- ~h ec ked

Ul l~ ti RID Jo. r,j rJ ;')71 o.IAGI<C ToC: N-:<1!1 >-1 )!:CL-!r<A.110Jl ~T :CC !t ( "" ~ OF S tiEU

- ~'~~~~~

~~~=='~-! r.lll f

n"= ,-_:'c'"~'~'~=-''"~"~''=~'~'"~'':o--c-o"'.-='":~""- ~o(J;'-c~"=-------' - EET

'=~~~~"-="- ~-~"~,,_-,!_0~-=-~~= = ==-'"' _!~~~OM CIT~

CO NTOUR IN7EFWAL 10 H. [ T NATI O N~l (i[Q(.Ir ri C V~R ll (:f! L DATUM OF 1 97~

TH IS '"lAI" C:OMI-' Lit:.i> WIT t-' NA H O ii ,l.l MAP ACCURACY STAND.~i1D ~
FOR SA L[ BY U.S. GEOLOG IC I'. I. SU/1\'t.Y. RES'JON.VIRGINIA 22092 A FO! 0 R Di:.SCRIB ING TOF'OGRM 'HIC M/.PS 1\ti!D S'fMilO LS !S A\'AI LA!lLE ON REQU t Sl'

,- -,

I

.

' '

;. ' } '\ C:;DRt~l \ '-.

\.___ -)

Ol.' ::lP.A~(, L~ , :~AtiL'l~,

ROAD CLASSi fiC AT ION

Pr ll' <ir"f lr1ghw~y _ h ~rd surface

Ligh!-dut~ road , hild 0 t
: m pro~eoJ su r:'ar.e _- - - - -

S.:>( Ofldary {l: ghwa)',
l1a rd surlace_

Unimrrrw::d ru~d... -~----- __

1U S Rr,~.-te

DOVElREL, GA.
N 0! 1 3 7 5 -Wft43 0//. ~
1973
AM 6 .(U4.7 11 NE - S ERIEZ I'S 45

Geologic Map of the Doverel Quadrangle, Georgia

Explanation
Detailed descriptions of rock umits included in text of Open File Report 07-1
Map Units

c::::::J Water

c::::::J Qal - Quarternary Alluvium JPoorly sorted silt, sand and gravel

c::::::J Ta- Miocene Altamaha Formmtion -massive rugillaceous sandstone

I

I Tsr- l'erliruy Sediments and Residuum- massiv<;; waxy chty ~md locally abundant cherl

C J Tcb- Lower to Middle Eocene~ Cla iborne Group- mnssi.vc to cross-bedded, line to t:onrsc sand and sandsto ne

IY'VI Cross Section

Core Ifole
~ ConlMcl (located approxi mately)

Geology by Mark D. Cocker
Dtgttlzed and digitall y compiled by rvttark D Cocker :rvlap projection , Albers Conic Equal A\reo NA 027
August, 2007 Supported by the US. GeologiCal Sun vcy, National Cooperative Geologic
Mapping Program, wtder assistance A'\.ward Agreement #OGHQAG0044

Cross-Section A - A' Doverel Quadrangle

~

Explanation
Alluvium (Holocene and Pleistocene) ~Variably micaceous, poorly sorted, fine- to coarse-grained sediment and variable amounts of organic matter deposited in cltannels, flood plains, and marshes_

~

Altamaha Formation (Miocene)- Massive, brick red, argillaceous, moderately indurated, fine-grained to gritty sandstone containing variable amounts of small, rounded, generally black, "ironstone" pebbles. A basal conglomerate that may contain chert residuum, iron-oxide cemented sandstone or iron-oxide crusts is usually presenL Unconformably overlies all other stratigraphic units at least to the Upper Cretaceous Providence Formation_ Forms a caprock that protects underlying softer, more easily eroded sediments and is the source for the best agricultural soils in this part of Georgia. May be extensively mot11ed in upper parts of exposures due to the dovmward migration of water and day_

~

Tertiary Sediments and Residuum (Eocene to Oligocene?) -Includes brown to orange, mottled, sticky clay and massive, whitish, locally fossiliferous chert fragments_ Clay may be massive or exhibit distorted, tine layering. Clay and chert fragments are commonly intermixed. This residuum may be the weathered equivalents of Eocene to Oligocene carbonate rocks. This unit is highly discontinuous in the map area.

I Tel> ,J

Claiborne Group (Lower to l\'liddle Eocene) -Massive to finely laminated, locally cross-bedded, white, light 1an to brick red, locally kaolinitic, fine- to coarse-brrained sand and poorly indurated sandstone. Unconfmmably overlies the Tuscahoma and Nanafalia Fonuations. Highly susceptible to rapid erosion.

~

Tuscaboma Formation (Upper Paleocene to Lower ILocene)- Non-fossil iferous, gray, red or purple interlaminated clay, silty clay, and fine quartzose sand. May locally be overlain by the Bashai Member of t:he Hachetigbee }"ormation consisting of light to dark greenish-gray, dominantly massive, well-sorted, vet)' fine- to fine-grained quartz and glauconitic sand.

NW
A
400
0a3
300 ~

114"'---1

Tsr
.':~ \

Ta

~- ~ - --.-- ~~-- '7-:" ~-~"" -<=- ~~--- " ,,

?

,- ~

. ,.....~ ----- ~-~ -- ~-=- -

'

-"
~
u rn c

if_

0a3

-/a"'

~ '

Horizontal Scale: 1" = 2000' Vertical Scale: 1' = 100'

Ta

-"'

Ta

//a

"-~-""'- - .. "----=

-r"u
~
u
f
~
-u"
0
c
f
-u"
a,;

SE
N
400

Ta

a03 1 3oo

I

-~,o~o-:o:~~-- ~ -- -- --:o;:-c-- =;-.,.,. - -,-,._-- :c___,-.~,- -:-- -~ cc----:-c'~ c .=i

200
t -.--~~--- ---h .

Tcb

~ -- - -2----

""- _-_. --~-"'~-:,. ---'-~----::._~-- .--- --

- -~---------- ----~...~- ---- - - ------

--~ - -

- -- -

- - - ----- - - '-

~--- . : . ~- -----. .~- - " "--- - -\ __.;._______._.. ;'- - -------

-.~4
:~-....~""""""" ~.,-

200

Tcb

Ttu

---~-"---~-----... -"-~--- ~-----" ~------ ----~---- ~--- ----- C ----- - - - - .-

_____ _ _ _ .__ ;._._ _ - -

--"' - - -

- - ---

- - -- - -- - - - " --- - - -- - - - - - - --

- c - ---...

Ttu