Hydrologic Significance of the Lithofacies of the Sparta Sand in Arkansas Louisiana, Mississippi and Texas

GEOLOGICAL SURVEY PROFESSIONAL PAPER 569-A Hydrologic Significance of the Lithofacies of the Sparta Sand in Arkansas Louisiana, Mississippi and Texas By J. N. PAYNE GEOHYDROLOGY OF THE CLAIBORN GROUP

GEOLOGICAL SURVEY PROFESSIONAL PAPER 569-A

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1968 UNITED STATES DEPARTMENT OF THE INTERIOR STEW ART L. UDALL, Secretary

GEOLOGICAL SURVEY William T. Pecora, Director

For sale by the Superintendent of Documents, U.S. Government Printing Office Washington, D.C. 20402 CONTENTS

Page Abstract.______Al Hydrology.--_--_------_-----_------_- A5 Introduction-______1 Permeability and transmissibility in relation to Purpose and scope.______1 geologic factors-______Acknowledgments. ______2 Recharge and discharge.______Geology-______2 Regional flow______Structure.______2 Chemical quality of water and relations to geologic and Thickness______3 hydrologic factors______Lithologic variations and interpretation of deposi- Chemical provinces-______10 tional environment.______3 Dissolved solids.______10 Maximum sand-unit thickness.______4 Extent of flushing of the Sparta Sand ______14 Conclusions.______14 Selected bibliography______15

ILLUSTRATIONS

[Plates are in separate case] PLATE 1. Section A-A'-A" showing correlation of the Sparta Sand and associated formations through the central part of Arkansas, Louisiana, Mississippi, and Texas. 2. Section B-B' showing correlation of formations, and dissolved-solids content, of Sparta aquifer in northeastern Louisiana, and southeastern Arkansas. 3. Structure-contour map on the base of the Sparta Sand in Arkansas, Louisiana, Mississippi, and Texas. 4. Map showing sand-percentage distribution and thickness of the Sparta Sand in Arkansas, Louisiana, Mississippi, and Texas. 5. Sections C-C' and D-D' showing variable thickness of continuous sand units in the Sparta Sand, northeastern Louisiana and southeastern Arkansas. 6. Map showing the maximum sand-unit thickness in the Sparta Sand in Arkansas, Louisiana, Mississippi, and Texas. 7. Map showing estimated coefficient of transmissibility of the total sand thickness of the Sparta Sand in Arkansas, Louisiana, and Mississippi. 8. Map showing the piezometric surface and the base of fresh ground water in the Sparta Sand in Arkansas, Louisiana, and Mississippi. 9. Map showing dissolved-solids content and chemical provinces of water in the Sparta Sand in Arkansas, Louisiana, Mississippi, and Texas. 10. Map showing cumulative thickness of fresh- water-bearing sand, and percentage of total sand thickness that is fresh­ water saturated, in the Sparta Sand in Arkansas, Louisiana, and Mississippi. Page FIGURE 1. Index map showing area of report---__-____-__--___-____----_---_------_------_ A2 2. Generalized section showing relation of regional geology and hydrology. ______-____--_-_---_-_-_----___-. 7 3. Electric logs of wells and chemical analyses of waters from the Sparta Sand in the Monroe, La., area showing variation in major chemical constituents at different stratigraphic positions within the formation. ______9 4. Graph showing relation of specific conductance to dissolved-solids content in waters from the Sparta Sand in Arkansas, Louisiana, Mississippi, and Texas ______11

TABLE

Page TABLE 1. Analyses of water from representative wells in the Sparta Sand- A12

GEOHYDROLOGY OF THE CLAIBORN GROUP

HYDROLOGIG SIGNIFICANCE OF THE LITHOFACIES OF THE SPARTA SAND IN ARKANSAS LOUISIANA, MISSISSIPPI, AND TEXAS

By J. N. PAYNE

ABSTRACT A study of the ground-water chemistry indicates that the The study of the geohydrology of the Sparta Sand is the initial areas of higher transmissibility have lower concentrations of phase in the investigation of the geohydrology of the Olaiborne dissolved solids than the areas of low transmissibility. On the Group. basis of anion ratios, the waters of the Sparta Sand are grouped The thicker sections of the Sparta Sand lie along the axes into three chemical provinces: the bicarbonate water province, of the Mississippi embayment and Desha basin. The area of the chloride water province, and the sulfate water province. maximum thickness, 1,100-1,200 feet, is in Claiborne and Warren The dissolved-solids content of waters from the Sparta Sand Counties, Miss., and Madison Parish, La. Local thickening or is closely related to the lithologic framework of the Sparta thinning over some structures indicates structural movement Sand area. Differences in water chemistry are attributed to during Sparta time. regional differences in the rates of ground-water movement. A sand-percentage map prepared from data derived from Interpretation of the data suggests that the channel deposits interpretation of electric logs indicates that the Sparta Sand have undergone a higher degree of flushing by fresh water than was deposited as a delta-fluvial plain complex in Arkansas, the interchannel deposits. Louisiana, and Mississippi. This complex shows a text-book example of a well developed channel pattern. The delta-fluvial- INTRODUCTION plain complex probably resulted from an ancestral Mississippi PURPOSE AND SCOPE River system. In most of Texas the sand-percentage map shows a pattern suggestive of offshore or near-shore bar deposition. Abundant electric-log and hydrologic data on the A map of the maximum sand-unit thickness shows the de­ gulf coast area of the United States are available for velopment during deposition of an interlacing channel pattern study and analysis to aid in understanding the relations in Arkansas, Louisiana, and Mississippi. In the channel areas the maximum thickness of the sand units may be as much as between hydrologic and geologic factors and delineating 350 feet; in the interchannel areas the maximum thickness the potential for ground-water development. The rela­ is generally less than 50 feet tions between hydrologic and geologic factors in aqui­ Coefficients of permeability and transmissibility for the fers can more accurately indicate the ground-water Sparta Sand vary widely in localized areas. In the channel- potential if they are studied on a regional basis. There­ sand area of Arkansas, Louisiana, and Mississippi, data suggest that the coefficient of permeability increases with an increase fore, a study of the formations of the Claiborne Group in maximum sand-unit thickness. These permeability values of Eocene age was begun in early 1961. The initial phase which depend on sand unit thicknesses, were used to prepare of this study describes and evaluates the relations of a map showing the transmissibility of the total sand thickness stratigraphy, structure, facies development, and de- of the Sparta Sand in Arkansas, Louisiana, Mississippi, and positional controls to the hydraulic characteristics of eastern Texas. The data on the map show a close relation be­ tween channel development and high transmissibility values. the Sparta Sand in parts of Arkansas, Louisiana, Mis­ The Sparta Sand is recharged by infiltration of water from sissippi, and Texas (fig. 1). Similar reports will be pre­ precipitation on the outcrop, by leakage from other aquiflers, pared for the Cockfield and Cane River Formations. and by seepage from streams. Natural discharge from the Sparta Sand takes place primarily by leakage through the Both electric-log data on oil and gas wells and on test overlying and underlying confining beds. In Texas, west-central wells and hydrologic data were used to prepare the Louisiana, and southeastern Mississippi the direction of flow geologic and hydrologic maps. The electric-log analysis of ground water is down the regional dip toward the gulf was initiated in areas of dense drilling where extremely coast geosyncline. In most of Arkansas, Louisiana, and Mis­ close control was available, and was then expanded sissippi the regional flow is toward the Mississippi River alluvial valley. In the channel-sand area of Arkansas, Louisiana, and systematically by running closed traverses of logged Mississippi the ground-water flow is governed by changes in sections into less densely drilled areas. Where possible transmissibility, which in turn reflects the lithology. the lithologic interpretation of these sections was veri- Al A2 GEOHYDROLOGY OF THE CLAIBORN GROUP shale, and minor amounts of lignite. The sand is com­ posed almost entirely of rounded to subrounded fine to medium quartz grains and is generally well sorted. There are a few layers of coarse sand and fine gravel (Brown, 1947, table 2, p. 60-64; Jones and Holmes, 1947, table 3, p. 37-38; Hewitt and others, 1949, p. 14). Glauconite, though fairly uncommon, occurs in sands at various stratigraphic positions in the formation, par­ ticularly in the upper part (Andersen, 1960; Born- hauser, 1947; Brown, 1947; DeVries and others, 1963; Harvey and others, 1961; Hewitt and others, 1949; Sellards and others, 1932, p. 651; Wendlandt and Knebel, 1929). The shales and clays are typically sandy to silty and gray to dark brown or black depend­ ing on the amount of included carbonaceous material. The correlations of the Sparta Sand as used in this report are shown in the sections through Texas, Louisi­ ana, Mississippi, and Arkansas (pis. 1, 2). As these correlations are based primarily on electrical character­ istics, they may not correspond exactly to formational boundaries that might be established by paleontological FIGURE 1. Location of report area. evidence, but they do define what may be considered as the Sparta hydraulic system and give a consistent interval for the calculation of sand content of the fied by studies of cuttings or core descriptions along system. with stratigraphic sections from nearby outcrops. This STRUCTURE method reduces the possibilities of making gross errors in correlation and interpretation. The pattern of litho- The structure of the Sparta Sand is shown by a con­ logic variability was mapped from the electric-log in­ tour map (pi. 3) of the base of the formation. As this terpretations and was used in the preparation of other study is concerned primarily with the regional geology geologic, hydrologic, and geochemical maps. and hydrology, faulting has been ignored except where The maps accompanying this report are the principal elevation changes are so great and so abrupt that a products of the study, and the discussion is merely an fault must exist, as in Bienville and Winn Parishes, elaboration of the data on the maps. Consequently, La., and in Nevada and Ouachita Counties, Ark. frequent reference to the maps is necessary for complete In south-central and southwestern Arkansas and understanding. north-central and northwestern Louisiana, the regional dip is to the east and southeast at 25-50 feet per mile ACKNOWLEDGMENTS toward and into the Mississippi embayment and the Desha basin. In southeastern Arkansas and north- Acknowledgment is made to the Louisiana Geological central Mississippi the dip is to the south, southwest, Survey, Department of Conservation; the Arkansas and west at about the same rate into these same struc­ Geological Commission; the Texas Water Commission ; tures. In south-central Louisiana and southern Missis­ and the Mississippi Oil and Gas Board for making sippi the influence of the gulf coast geosyncline is dom­ available their log files. Acknowledgment is also made inant, and the regional dip is generally to the south at to the personnel of the district offices of the Water Ke- 50-100 feet per mile. In Angelina, Jasper, Newton, sources Division of the U.S. Geological Survey in Sabine, San Augustine, and Tyler Counties, Tex., the re­ Arkansas, Louisiana, Mississippi, and Texas for sup­ gional dip is to the south and south-southwest at about plying hydrologic and geologic information and for 100 feet per mile from the Sabine Arch into the gulf making many helpful suggestions and criticisms. coast geosyncline and the east Texas syncline. From GEOLOGY Houston County, Tex., southward to Webb County, Tex., the regional dip is to the southeast at 150-200 feet The Sparta Sand (Vaughan, 1895, p. 225-226, 1896, per mile into the gulf coast geosyncline. p. 25-26; Spooner, 1926, p. 236-237) consists of varying The major structural features that developed consid­ amounts of sand interstratified with silt, clay, and erably during Sparta time are the Mississippi embay- HYDROLOGIC SIGNIFICANCE OF THE LITHOFACIES OF THE SPARTA SAND A3 ment, Desha basin, Sabine arch, and Jackson dome, and, paction of shales and clays surrounding massive sand to a lesser extent, the Monroe uplift and the LaSalle bodies or areas containing a high percentage of sand. arch. These developments are indicated by the thicken­ Such variations in thickness are generally indiscernible ing or thinning of the Sparta over these structures. The on maps drawn on a regional scale. However, some of downwarping of the Mississippi embayment during the thick elongated areas in Madison, Richland, and Sparta and post-Sparta time is shown by the marked Tensas Parishes, La., and Jefferson County, Miss., steepening of the dip on the basinward flanks of Jack­ may result from differential compaction or from son dome and similar structures. Minor structural fea­ downcutting. tures are associated with the Tinsley oil field, Yazoo County, Miss., the Madisonville oil field, Madison LITHOLOGIC VABIATIONS AND INTEBPBETATION County, Tex., and other oil fields and a number of salt OF DEPOSITIONAL ENVIBONMENT domes (pis. 3, 4). Faulting such as is shown on pi. 3 The lithology of the Sparta Sand is highly variable occurred throughout the gulf coast area. both vertically and laterally. Predominantly sandy sec­ tions grade into predominantly shaly sections within THICKNESS very short distances (pis. 1, 2, 4). A good method of The thickness of the Sparta Sand generally exceeds creating some order from such variability is to prepare 800 feet along and near the axes of the Mississippi em­ a sand-percentage map on which the ratio of the thick­ bayment and the Desha basin in 'southeastern Arkansas, ness of sand in the formation to the thickness of the eastern Louisiana, and western Mississippi (pi. 4). The formation is expressed as a percentage; that is: maximum thickness, 1,100-1,200 feet, occurs in Clai- a j , total thickness of sand .... nn borne and Warren Counties, Miss., and Madison Parish, hand percentage^ , ,,, . . j^ -. X100. r & total thickness of formation La. Eastward from the axes of the Mississippi embay­ ment and Desha basin, the Sparta Sand thins rapidly The values calculated for each logged section can then to only 250-300 feet in central and east-central Missis­ be plotted on a map and grouped by appropriate per­ sippi and 100-150 feet in southeastern Mississippi. centage increments. This method was used in the prep­ Westward from the axes the thinning is more gradual; aration of the sand-percentage map (pi. 4) of the 'Sparta the Sparta is 400-600 feet thick in south-central and Sand using increments of <10 percent, 10-30 percent, southwestern Arkansas and central and west-central 30-50 percent, 50-70 percent and >70 percent. As previ­ Louisiana (pi. 4, sheet 1). In eastern Texas the forma­ ously mentioned, this work was begun in areas of good tion generally is 300-500 feet thick, but it thins to control, where the percentage values formed definable 100-200 feet in Fayette and Gonzales Counties and patterns that could reasonably be extended into areas maintains a rather constant thickness of 100-150 feet to of less control. the southwestern extremity of the area mapped in Webb On the basis of the distribution of sand-concentration County, Tex. (pi. 4, sheet 2). patterns, the Sparta can be divided into two areas which Local variations in thickness are common and in seem to have had different depositional environments. some places pronounced, as in the Jackson, Miss., area. One area includes Louisiana, Mississippi, southern Ar­ The more obvious of these variations are associated with kansas, and eastern Texas, and the other extends from localized structural features which were developing Grimes to Webb Counties, Tex. during the period of Sparta deposition. Such structures Louisiana, Mississippi, southern Arkansas, and east­ are the Jackson and Tinsley domes of Mississippi, parts ern Texas. The most conspicuous characteristic of the of the Monroe uplift in Morehouse and Ouachita Par­ lithologic pattern of the southern Arkansas-Louisiana- ishes, La., and Sharkey County, Miss., and the Desha Mississippi-eastern Texas area is the well-developed basin in Drew and Lincoln Counties, Ark. Variations lineation of sand concentrations in a general northerly associated with structural growth are less pronounced direction, presumably normal to the orientation of the over some of the oil-field structures in southern Sparta shoreline. The pattern of sand distribution in Ouachita, southern Bradley, and northern Union this area was probably created by a system of anastomos­ Counties, Ark., and in Madison County, Tex. Additional ing, constantly shifting stream channels and interlacing examples of local variations in thickness can be found lakes, marshes and swamps such as would be developed by comparing the thickness map of the Sparta Sand in a large deltaic-fluvial plain. The frontal edge of this with oil and gas maps. Some local variations in thick­ large arcuate former delta extends from Wayne County, ness of the Sparta result from cut and fill channels at Miss., southwestward through southeastern Louisiana the base of the Sparta that penetrate the upper part of probably as far as northern Pointe Coupee, St. Landry, the Cane River Formation, and from differential com­ and Alien Parishes, and thence west-northwestward A4 GEOHYDROLOGY OF THE CLAIBORN GROUP into Sabine County, Tex. This delta represents the is not apparent in the area from Grimes County to record of an ancestral Mississippi Eiver system that Webb County, Tex. In this area the long axes of the existed probably in Sparta and possibly in much of sand-concentration patterns and the sand bodies are Claiborne time. The channel deposits in Houston, Madi­ parallel to, rather than normal to, the postulated Sparta son, and other counties in east Texas probably represent strand line. Another point of contrast between the two smaller streams. This interpretation conforms with the areas is the distance from the outcrop area to the limits ideas of earlier investigators who did surface work in of continuous sand deposition, sometimes called the smaller areas (Spooner, 1926; Huner, 1939). "shale-out" line. If measured normal to the regional Although the Sparta Sand is predominantly of con­ dip in Louisiana, the distance generally ranges from tinental origin in the delta area, brief local invasions of 50 to 200 miles; in the area from Grimes County to Mc- the sea repeatedly covered low-lying areas of the land Mullen County, Tex., the distance generally ranges mass, particularly during later Sparta time. These in­ from 14 to 50 miles. This difference is accounted for not vasions are indicated by the fossiliferous and glau- only by differences in degree of regional dip and thick­ conitic sand and shale beds in the Sparta (Andersen, ness of the Sparta but also by more extensive sand dep­ 1960, p. 87-88; Chawner, 1936, p. 72; DeVries and oth­ osition in the delta area. ers, 1963; p. 14; Harvey and others, 1961, tables 7, 8, The thickness characteristics of the Sparta Sand also and 9; Hewitt and others, 1949, p. 11-14; Huner, 1939, differ in the two areas. From Grimes County southwest- p. 83; Jones and Holmes, 1947, p. 14; Maher and Jones, ward the thickness is uniform, but in Arkansas, Loui­ 1945, p. 40-41; Spooner, 1926, p. 236; Wang, 1952, p. siana, and Mississippi it is extremely variable. An 56-58). interpretation of the orientation of the sand bodies par­ Eegionally, the numerous long meandering areas that allel to the strand line, the constant thickness of the contain at least 50 percent sand represent "flow-ways," Sparta interval, and the distance from the outcrop to which remained areas of channel development through­ the "shale-out" line all suggest that the subsurface out most of Sparta time. (Compare pis. 4 and 6.) Such Sparta sands in the central and southern gulf coast re­ an area extends from Drew County, Ark., through west­ gion of Texas are predominantly near-shore bar and ern Ashley County, Ark., western Morehouse Parish, beach deposits rather than fluviatile deposits as in out­ La., and southward into western Franklin Parish, La. crop areas in Louisiana (Spooner, 1926, p. 236-237; These areas were the sites of channel formation at differ­ Huner, 1939, p. 76-82). This interpretation is supported ent times during the deposition of the Sparta and are by Sparta-Stone City relations in Leon County, Tex. similar to the channel-development areas along the pres­ (Stenzel and others, 1957, p. 20), where the nonfossil- ent courses of the Ouachita and Mississippi Eivers and iferous continental beds of the Sparta interfinger with, other streams (Fisk, 1944, pi. 2). The associated areas and grade upward into, the fossiliferous marine beds of that contain less than 50 percent sand probably repre­ the Stone City of Stenzel (1938). This suggests that the sent interchannel swamp, marsh, and lake areas where strand line was near. The interpretation is further sup­ the finer detritus and vegetal material accumulated. ported by Sellards, Adkins, and Plummer's (1932, p. Large water supplies can be developed in the areas that 654) description of the Sparta Sand. contain at least 50 percent sand. In areas of sparse drilling, future development of MAXIMUM SAND-UNIT THICKNESS closer control should show a greater degree of lateral A study of electric logs indicated that a map of the variability than is shown by present maps. However, thickness of the thickest vertically continuous sand the general pattern of channel deposition will probably body for convenience, designated the maximum sand- remain, and any revisions will be significant only in unit thickness (pi. 5) of the Sparta Sand would aid specific and detailed local studies. in better understanding the mode of deposition, more Eegionally, the sand content of the Sparta generally accurately locating channel paths, and understanding decreases from southern Arkansas, northern Louisiana, some of the variations in hydraulic characteristics. In and northern and central Mississippi southward toward general, the maximum sand-unit thickness map (pi. 6) the margins of the delta (pi. 4). This decrease is prob­ is similar to the sand-percentage map; thick sand bodies ably accompanied by an increase in the occurrence of usually occur in areas in which the total percentage of marine interbeds as the area of marine environment is sand is high. However, there are several exceptions approached (Bornhauser, 1950, p. 1892). where individual units more than 100 feet thick extend Central and southern Texas gulf coast. The channel into areas where sand percentage values are low (30-40 pattern that is so conspicuous in Arkansas, Louisiana, percent). In some areas the sand concentration may be and Mississippi and less conspicuous in eastern Texas 50 percent or more and the maximum sand-unit thick- HYDROLOGIC SIGNIFICANCE OF THE LITHOFACIES OF THE SPARTA SAND A5 ness may be only 30-50 feet. The maximum sand-unit PERMEABILITY i AND TRANSMISSIBILITY 2 IN thickness is a major factor in the evaluation of the po­ RELATION TO GEOLOGIC FACTORS tential ground-water supply. (See discussion on per­ Because of the variable lithologic framework of the meability and transmissibility.) Sparta, permeability values differ greatly within small Louisiana, Mississippi, southern Arkansas, and east­ areas. For example, the field coefficient of permeability ern Texas. The axes of thickening of the maximum determined from pumping tests in northeastern Oua- sand units in Arkansas, Louisiana, Mississippi, and chita and southwestern Morehouse Parishes ranges from eastern Texas (pi. 6, sheet 1) have been plotted to aid 130 to 890 gpd per sq ft (gallons per day per square in reading the map. These axes also emphasize the inter­ foot) in a distance of about 6 miles. In a number of lacing channels that are similar to the meander patterns places the permeability of the same sand bed may vary of present-day streams in areas of heavy alluviation as much as 200-300 gpd per sq ft within 1 mile. (Fisk, 1944, pi. 2). Within the channel areas the maxi­ Notable local variations in transmissibility occur in mum sand units range from 100 to 350 feet in thickness, the Jackson area, Hinds County, Miss., in eastern Winn but in the interchannel areas they generally range from Parish, La., and in southwestern Ashley County and 10 to 50 feet. Maximum sand units 100 feet or more thick northwestern Desha County, Ark., where the differences may coalesce or diverge, and as entities they are gener­ in transmissibility of the total sand thickness of the ally of limited aeral extent, but the effect of overlap Sparta Sand are as much as 200,000 gpd per ft (pi. 7). gives almost continuous interconnection for fluid flow The relations of permeability and porosity to such (pi. 5). These thick sand bodies can be traced for several factors as grain size, grain shape, arrangement, sorting, miles parallel to the channel axes (section D-D'), but and packing were summarized by Meinzer (1923, p. 2- normal to this direction they are of limited aeral extent 28, 63) and Pettijohn (1957, p. 81-89). Permeability (section C-C'). They may occur at any stratigraphic and transmissibility are directly related to the lithologic position in the Sparta, but most are in the lower two- variations of the Sparta Sand and, thus, are indirectly thirds of the section. related to its mode of deposition. The direct relations Central and southern Texas gulf coast. From are major factors in the consideration of the hydraulic Grimes County, Tex., southwestward, the axes of thick­ cliaracteristics of the formation. ening of maximum sand units are not long (pi. 6, sheet In the channel area of Arkansas, Louisiana, and Mis­ 2) and are normal to the regional dip. The limited ex­ sissippi, high coefficients of permeability do not neces­ tent and the orientation of the maximum sand units are sarily occur in areas in which the percentage of sand not conducive to extensive downdip migration of fresh is high. These high coefficients of permeability are usu­ water. ally in areas where the maximum sand-unit thickness HYDROLOGY is greater than 100 feet. Therefore, the maximum sand- The Sparta Sand is one of the major sources of unit thickness may be related to the coefficient of perme­ ground water in southern Arkansas, northern and ability of the sand. Coefficients of permeability deter­ north-central Louisiana, western and central Missis­ mined from pumping tests and specific-capacity tests sippi, and eastern Texas as far west as Burleson County. of wells were compared with the thickness of the sand Large quantities of soft water of low dissolved-solids section in which the well was screened. Sufficient data content (pis. 7, 9; table 1) are available from the Sparta are lacking to reach any firm conclusions, but the com­ throughout much of this area. However, from Burleson parison strongly indicates that the coefficient of per­ County southwestward in Texas the Sparta Sand is of meability varies directly with the sand thickness. Such minor importance as an aquifer because it contains fresh a relation is reasonable for sands deposited in channels water only in a small area, yields are low, and the water because the thicker sand units would lie along the lines is hard and has a high concentration of dissolved solids of persistent flow where velocities would be higher than (pi. 9; table 1). in the marginal areas. Therefore, the sand in the thicker When considering the Sparta Sand as an aquifer, one units would be cleaner, generally better sorted, and must realize that the aquifer system is made up of sev­ 1 The coefficient of permeability is defined as the rate of flow of water, in gallons eral imperfectly connected sand bodies, any one of per day, through a cross-sectional area of the aquifer 1 foot square under a hydraulic which may act locally, and for short periods of time, as gradient of 100 percent, or 1 foot per foot, at a temperature of 60°F (Meinzer and Wenzel. 1942, p. 452). a separate hydraulic unit. Over longer periods of time * Transmissibility of an aquifer is expressed (Bredehoeft, 1964, p. D168) as: and larger areas, these units act as an integral part of where the unified Sparta hydraulic system and ultimately i=l, 2, 3 ... n layers of differing permeability, form an element of the regional hydrologic system of T= transmissibility, Ki= permeability of the i layer, the gulf coast. A/,=thickness of the i layer. 269-725 68 2 A6 GEOIIYDROLOGY OF THE CLAIBORN GROUP somewhat coarser than that in the thinner units along where only one massive sand unit occurs, but frequently the margins of the channel. The correlation between several massive sand units of equal or nearly equal permeability and maximum sand-unit thickness is suffi­ thickness are present in the section (pi. 5). This obvi­ ciently good to warrant the use of different average ously causes differences in the transmissibility and permeabilities for sand bodies of different thicknesses maximum sand-unit thickness maps (pis. 6 and 7). in calculating transmissibility, rather than an overall The foregoing discussion of the relation between average of the coefficients of permeability. Fifty-foot sand-unit thickness and the coefficients of permeability categories of sand-unit thickness were selected; the and transmissibility in stream-channel deposits does not average coefficient of permeability for each category apply to offshore bars, beach bars, and dune sands, is as follows : where the agents and mechanics of deposition are differ­ Average coefficient Sand thickness of permeability ent. Southwest from Buiieson County, Tex., much of (ft) (gpd per sq ft) the Sparta Sand appears to be of the offshore bar or =^50 ______* 225-250 51-100 ______1 325-350 beach-bar type, but sufficient hydrologic data are lack­ 101-150 ______* 450-500 ing for the determination of the relation of the thick­ ^151 ______600 ness of the beds of sand to coefficients of permeabiilty 1 The higher values were used in parts of Arkansas and Mississippi and transmissibility. where available data indicate a generally higher coefficient of perme­ ability than in Louisiana. RECHARGE AND DISCHARGE These coefficients of permeability were then used to cal­ culate the transmissibility of the total sand thickness of The Sparta Sand is recharged by direct infiltration the Sparta sands. The thickness of sand within each of in the outcrop area and by leakage from alluvium and the 50-foot categories was multiplied by the appropriate from other aquifers with higher heads. average coefficient of permeability, and the products The rainfall is high in Louisiana, Mississippi, and were added to obtain the transmissibility of the total southern Arkansas, and the contribution of water to the sand thickness at each location. The results were then Sparta aquifer by direct seepage from streams is there­ used to prepare a map showing the transmissibility of fore negligible because most of the streams serve as the Sparta Sand in the channel sand area of Arkansas, drains for ground-water discharge. In Texas, where Louisiana, and Mississippi (pi. 1} . rainfall is relatively low, the infiltration of water from The use of the different average coefficients of permea­ streams may be appreciable. bility for different thicknesses of sands seems to give Discharge from the Sparta Sand occurs by with­ a more realistic coefficient of transmissibility than the drawal from wells and by natural discharge. The effects use of an overall average value. A simple example will of large withdrawals from wells are evident in the illustrate the differences that may occur in using the two Hodge-Jonesboro area, Louisiana, in Jackson, Miss., in approaches. Assume that we have a total sand thickness El Dorado, Ark., and near Monroe, La. (pi. 8). Natural of 300 feet, composed of 2 sand units 150 feet thick near discharge takes place primarily by leakage from the well A and 10 sand units 30 feet thick near well B. Sparta Sand through the overlying and underlying using the variable permeability values we get a trans­ confining beds. missibility value of 135,000 gpd per ft. (150X450X2) REGIONAL FLOW near well A and a transmissibility of 67,500 gpd per ft. (30X225X10) near well B. If an overall average is In a formation having the geologic framework of the used, the same transmissibility value is obtained for Sparta Sand, alternating sand and shale bodies that both wells A and B. The latter approach not ony dis­ have an appreciable regional dip, the bulk of the ground agrees with the results from pumping tests but also water available even in the outcrop area, is confined with certain chemical data. (See section on quality of above and below by relatively impermeable beds. water.) The flow of water ia an artesian aquifer occurs be­ The close relation between channel sand thickness and cause of the difference in head. In Texas, along the higher transmissibility values is illustrated by compar­ south flank of the Sabine uplift in Louisiana, and in ing plates 6 and 1. Certain minor deviations of maxi­ southeastern Mississippi, the direction of flow is gen­ mum transmissibility and maximum sand-unit thick­ erally down the regional dip toward the gulf coast ness occur because of inherent properties of the maxi­ geosyncline. In most of Arkansas, Louisiana, and Mis­ mum sand-unit thickness map. Only the value for the sissippi, the major focus of discharge is the Mississippi thickest sand unit in any given section is shown on the River alluvial valley. The regional direction of flow is maximum sand-unit thickness map (pi. 6). This value inferred from the water-level contours (pi. 8), the gen­ may be satisfactory for calculating transmissibility eral increase in dissolved-solids content, and the limits HYDROLOGIC SIGNIFICANCE OF THE LITHOFACIES OF THE SPARTA SAND A7 of fresh water downdip in the aquifer (pis. 8, 9, 10; is the westward offset of the alluvial valley relative to fig. 2). the structural axis of the Mississippi embayment. Be­ The relation of recharge, discharge, and regional flow cause of this offset and the effects of the Monroe uplift, to the geology and to the piezometric surfaces is shown the depth to the Cockfield and Sparta aquifers in the in figure 2, which is a generalized section from Bienville area of discharge in eastern Louisiana is much less than Parish, La., to Jasper County, Miss. that in western Mississippi. In the area shown in figure 2, water from precipita­ With these factors in mind, a reasonable interpreta­ tion that falls on the upland areas of the Cockfield and tion of the flow pattern in the systems can be made. Sparta enters these formations either directly or by (See directional arrows in figure 2.) Normally, water downward percolation through surficial material. moves downdip in the formations, but where the eleva­ Within short distances after entering these formations, tion of the water levels in the Cockfield is different from the water is in an artesian system, as it is confined above that in the Sparta, the water moves vertically and causes and below either by the interbedded shales of the Cock- a generalized regional flow pattern as shown in figure field and Sparta Formations themselves or by the clays 2. The regional flow pattern is similar to that dia­ and shales of the associated Cane River and Cook Moun­ grammed and discussed by Le Grand (1964, fig. 4, p. tain Formations and Vicksburg and Jackson groups. In 185). The areas of recharge for the Sparta are between the recharge area the piezometric surface in the Cock- the base of the formation in the outcrop areas and the field is higher than the piezometric surface in the points of intersection of the Sparta and Cockfield Sparta. The Cockfield Formation, however, is more ac­ piezometric surfaces on both sides of the Mississippi cessible to the regional discharge area in the valley; alluvial valley. (See fig. 2.) The principal area of nat­ consequently, the piezometric surface in the Cockfield ural discharge is between the two points of intersection. is more steeply inclined than that in the Sparta. Near Together, the flow components produce a markedly the discharge area the relative positions of the two asymmetrical flow pattern that contrasts with the sym­ piezometric surfaces are reversed. Furthermore, the re­ metrical structural pattern of the Mississippi embay­ charge areas of the Cockfield and Sparta Formations ment. The zone of flushing extends to a much greater in Mississippi are considerably higher than those in depth on the east flank of the embayment than on the Louisiana; thus, the piezometric surface is generally west flank. (See pi. 8, fig. 2, and section on quality of higher on the east side of the alluvial valley than on the water.) The saline-water core, 10,000 ppm (parts per west. Another major factor affecting the regional move­ million) dissolved solids, perches on the western limb ment of water in the Cockfield and Sparta Formations of the Mississippi embayment. Thus, an updip compo-

roj^^Lsu-^ai J 50Q ,

SEA 'LEVEL

500'- - 500'

1000'- - 1000' 10,000 ppm _____ o\ General direction of water movement sVft ^- ~""~*^? -1500' 1500'- X^ " * \\ ~ o ...... \^ A ^ |____ j^ Piezometric surface of Cockfield Fm. Monroe0 \ ovicksburgl k 7 2000' - * ^X Piezometric surface of Sparta Sand 2000' * \\v TEXAS I looo- ! Np- \. x 3000 2500'- I PPm | -2500' Zones of dissolved solids Concentrations., in parts per million (pp in water contained in Sparto Sand 3000' 3000'

FIGURE 2. Relation of regional geology and hydrology. A8 GEOHYDROLOGY OF THE CLAIBORN GROUP nent of movement exists on the east side of the saline- to the orientation of the sand beds; therefore, the flow water core. (See fig. 2.) is retarded by the shaly beds. In addition, there is no This hydraulic system has probably existed since post- focal line of discharge similar to the Mississippi allu­ Oligocene or pre-Pleistocene time. Repeated fluctua­ vial valley. Discharge occurs by slow upward leakage tions in sea level accompanied by periods of stream deg­ through a thick section of Cook Mountain clays and radation and aggradation and consequent changes in shales and, in places, a shaly Cockfield section. The re­ water levels have probably occurred since Sparta time. sults of a study of water levels in Wilson County, Tex. However, the timespan since the inception of the sys­ (Anders, 1957, table 6), indicate that the piezometric tem is so long that these fluctuations of relatively short surface in the Sparta a short distance downdip from the duration have left no recognizable marks on the regional outcrop is higher than that in the overlying Cook Moun­ pattern. Local effects of pumping on this regional flow tain and Cockfield, which indicates that upward leak­ pattern have been negligible. age from the Sparta starts within very short distances In the channel-sand area of Arkansas, Louisiana, and from the outcrop area. Downdip movement is limited Mississippi, the rate of flow varies with the lithology. by the rapid pinchout of permeable beds of any ap­ In the high-shale-content areas, the sands form a dis­ preciable thickness (pis. 4, 6). As a result of these fac­ connected or imperfectly connected system where the tors, downdip flushing of the sands by fresh water has flow is retarded by an intervening series of shale or silt been extremely limited. beds of low permeability. Where the section is pre­ Other major factors need further study. Among these dominantly sand, particularly in the channels where are the relations of the lithology of the overlying Cook massive overlapping sands occur (pi. 5), the slight to Mountain and Cockfield Formations to that of the moderate reduction in the premeability of the interven­ Sparta, the thickness of the Cook Mountain and Cock- ing beds does not affect the rate of water movement as field, and the differences in head between the Sparta and much as in the areas where the sand bodies are com­ the Cockfield. These factors are of particular signifi­ pletely enclosed by shales. Another major factor affect­ cance in the area of natural discharge because any factor ing the regional flow is the orientation of the channel that increases the discharge will accelerate the movement sands with respect to the direction of regional flow. For of water from the recharge area where there is ample example, in Claiborne, Union, Morehouse, and Ouachita supply to counterbalance the loss by discharge. To il­ Parishes, La., channels are oriented in two dominant lustrate the significance of what is implied, let us as­ directions. One trends east-northeast and virtually par­ sume that a predominantly sandy section of the Cook allels the direction of regional flow. The other trends Mountain and Cockfield Formations overlies one of the north and is nearly normal to the direction of regional favorably oriented high-transmissibility channels of flow. (Compare pis. 4,6,7, and 8.) In the east-northeast- the Sparta Sand in the area of discharge into the alluvial trending channels the water moves from the recharge valley of the Mississippi River. In such a system an area to the discharge area with little restriction by shale effective conduit would be formed from the area of or silt barriers, but in the north-trending channels the recharge to the area of discharge. This conduit would flow of the water is impeded by the rather extensive allow for an accelerated rate of discharge and a conse­ shaly areas that lie across the direction of regional wa­ quent accelerated rate of movement of water, which ter movement. The differences in rate of movement have would result in a more thorough flushing of the Sparta had, over the period of time involved, a pronounced in­ along this flow path than elsewhere in the aquifer. fluence on the degree of flushing, as can be seen by com­ CHEMICAL QUALITY OF WATER AND RELATIONS TO paring the map of dissolved-solids content (pi. 9) with GEOLOGIC AND HYDROLOGIC FACTORS the map showing the maximum sand-unit thickness and transmissibility (pis. 6, 7). The dissolved-solids content The relations of the regional chemical variations of in the channels parallel to flow is appreciably lower water in the Sparta Sand to geologic and hydrologic than that in the channels normal to flow. In both chan­ factors has been analyzed through the use of available nel areas the dissolved-solids content is lower than in chemical analyses. These data were supplemented by the adjacent shaly interchannel areas. Similar exam­ calculations of dissolved-solids content from electric ples of different degrees of flushing occur throughout logs to interpret the major regional chemical character­ the area, particularly in Hinds and Warren Counties, istics of the water. Miss., Union County, Ark., and Houston and Walker As a prelude to any discussion of water quality, one Counties, Tex. must realize that the analyses represent only water from The regional flow in the bar-sand area of Texas (pis. the zone sampled and are not necessarily indicative of 4, 0) is down the dip of the Sparta Sand and is normal the water chemistry in other zones of the Sparta aquifer HYDROLOGIC SIGNIFICANCE OF THE LITHOFACIES OF THE SPARTA SAND A9 system. Therefore, in the marginal areas of any par­ up the Sparta system. This occurs in the Monroe, La., ticular water province, waters of different types would area, where waters from different sands in the same well probably be found in the several sand units that make have been analyzed (fig. 3).

City of Monroe test 3 Sec. 6, T. 18 N., R. 4 E. Blevins water wells Ouachita Parish, La. City of Monroe test 1 Depth Sec. 52, T. 18N..R.4E., in feet Ouachita Parish,La. Self-potential Resistivity (ohms m 2/m) (millivolts) 50 100 -1201+\ Top Sparta Sand "Top Sparta Sand Resistivity (ohms m 2/m) -Analysis of water I 200 'from depth of 231-241 ft 100 (in parts per million) Calcium 3.2 Magnesium 1.7 Sodium 271.0 Potassium 4.8 Carbonate 20.0 300 Bicarbonate 522.0 Sulfate 2.6 Chloride 100.0 Analysis of water Dissolved from depth of 315 ft solids 684.0 (in parts per million) HCO, Calcium 2.8 Magnesium .7 C1+SO4 Sodium and Analysis of water potassium 209.0 400 from depth of 369-379 ft Carbonate 43.0 (in parts per million) Bicarbonate 336.0 Calcium 3.3 Sulfate 7.0 Magnesium 2.0 Chloride 76.0 Sodium and Dissolved potassium 200.0 solids 554.0 Carbonate .0 HCO, =&0 Bicarbonate 335.0 500 Sulfate 2.6 C1+S04 Chloride 123.0 Dissolved solids 688.0 HCO3 = 1.6 C1 + SO4 ^Analysis of water 600 from depth of 474-484 ft (in parts per million) Calcium 2.4 Magnesium 1.5 Sodium 232.0 Analysis of water Potassium 5.9 from depth of 654 ft Carbonate 9.8 (in parts per million) Bicarbonate 364.0 700 Sulfate Calcium 1.0 .8 Chloride Magnesium .3 147.0 Dissolved Sodium and potassium 176.0 solids 646.0 HCOS Carbonate 18.0 = 1.5 Bicarbonate 240.0 C1 + SO4 Sulfate 1.2 "Analysis of water Chloride 112.0 800 from depth of 725-735 ft Dissolved (in parts per million) solids 448.0 Calcium 1.2 HC08 Magnesium .72 = 1.4 C1 + SO4 Sodium 383.0 Potassium 4.8 Carbonate 28.0 Bicarbonate 353.0 Sulfate 2.1 Chloride 358.0 Dissolved solids 984.0 HC03 = 0.6 Cl+SOi FIGURE 3. Electric logs of wells and chemical analyses of waters from the Sparta Sand in the Monroe, La., area, showing the variation in major chemical constituents at different stratigraphic positions within the formation. A10 GEOHYDROLOGY OF THE CLAIBORN GROUP

CHEMICAL PROVINCES Mississippi, aided by the more favorable orientation of many of the high-transmissibility channel areas in rela­ Only the major constituents of the dissolved solids tion to the direction of flow, has increased the degree in water from the Sparta (table 1) are considered in of flushing on the east side of the valley. (See pis. this report. Regionally, sodium is the dominant cation. 6,7,10.) Calcium and magnesium occur in appreciable amounts Chloride water province. This province is that area only in very small areas. The anions, on the other hand, where chloride : bicarbonate + sulfate 1. In Texas occur in rather well defined provinces. As suggested by it includes all of the Sparta Sand except for limited Hem (1959, p. 155-156), the following chemical ratios areas in, and short distances downdip from, the out­ were studied in terms of equivalent parts per million: crop (pi. 9). In Louisiana it is generally confined to the sulfate: chloride + bicarbonate; bicarbonate: chloride + downdip area of the Sparta and to the saline-water sulfate; chloride: bicarbonate+sulf ate. The resulting tongue, which generally coincides with the area overlain values were plotted on a map (pi. 9). Examination of by the Mississippi valley alluvium in eastern Louisiana these data showed that the waters of the Sparta can be and southeastern Arkansas. The chloride type waters grouped into three rather well defined chemical prov­ generally represent areas of discharge where the domi­ inces a bicarbonate water province, a chloride water nant component of flow in the Sparta is upward (pi. 2, province, and a sulfate water province on the basis of fig. 2), and they therefore lie beyond the limits of ex­ the relations between the anions. tensive flushing by fresh water. (See pis. 8, 9, 10.) Bicarbonate water province. This province is that Sulfate loater province. Southwestward from Burle- area where bicarbonate : chloride + sulfate ^ 1. It son County, Tex., along the Sparta trend to Webb covers central and western Louisiana, all but the south­ County, sulfate may constitute up to 50 percent or more eastern part of southern Arkansas, virtually all of of the total anion content of the waters (table 1, well Mississippi, and small areas in the updip part of the TWn-4). The ratio value arbitrarily chosen for defini­ Sparta in Texas. In the downdip areas, the sands of tion of this province is 0.25 (sulfate : chloride + bicar­ the Sparta may contain mixed bicarbonate-chloride bonate ^ 0.25). The sulfate water province lies along, waters having varying percentages of these anions (fig. and slightly downdip from, the outcrop area of the 3). Updip from the bacarbonate water-chloride water Sparta (pi. 9). It coincides closely with an area in which boundary, toward the recharge area, the bicarbonate the formations overlying and underlying the Sparta anion becomes more and more predominant until it is Sand contain gypsum and gypsiferous clays (Alexander virtually the only anion present. This is illustrated by and others, 1964, p. 34-35 and 43^6). The sulfate con­ a comparison of the analyses for wells LMo-2, LOu-2, tent can probably be attributed to the solution of gyp­ LOu-1, LL-1, LL-3, LL-2, MW-1, MW-2, MH-1, and sum by waters passing through these gypsiferous for­ MK-1 (table 1 and pi. 9). mations and the soils derived from them. The dispersion The bicarbonate distribution seems to be a function of these salts downdip in the Sparta would be relatively of rate of water movement and of time. That is, the slow because the regional downdip rate of flow is very greater the degree of flushing the greater the proportion slow. of bicarbonate. This relation is indicated by the position of the line where bicarbonate : chloride + sulfate = I DISSOLVED SOLIDS relative to the limits of fresh water as delineated by the The dissolved-solids content of water is one of the 1,000-ppm minimum-dissolved-solids line on plate 9. most effective chemical tools that can be used to under­ The boundary of the bicarbonate water province is, in stand the relations of water movement, variations of general, considerably updip from the limit-of-fresh- chemical quality, and the influence of geologic factors water line in Louisiana, but in Mississippi the bicar­ on water movement. The relation of the dissolved-solids bonate line is generally downdip from, or coincides content to the specific conductance of water from the with, the limit-of-fresh-water line. The relative posi­ Sparta Sand is remarkably constant (fig. 4), even in tions of the bicarbonate and limit-of-fresh-water lines the higher ranges of concentration (^ 3,000 ppm). in Louisiana and Mississippi coincide with differences Because of this relation, electric logs can be used to in head in the two States as reflected by the slopes of compute dissolved-solids content. The electric logs pro­ the piezometric surfaces (pi. 8, fig. 2). The water level vide extensive regional control for computing dissolved- in Mississippi is 100-150 feet higher in the recharge solids contents in formational waters. area than the water level in a corresponding position A satisfactory method of computing the dissolved- in Louisiana. Thus, the steeper hydraulic gradient in solids content of water from the long-normal curve of HYDROLOGIC SIGNIFICANCE OF THE LITHOFACIES OF THE SPARTA SAND All

100,000 I 1 I I FT

10,000

1000

100 i I I I I 100 1000 10,000 100,000

SPECIFIC CONDUCTANCE, IN MICROMHOS PER CENTIMETER AT 25° CENTIGRADE FIGURE 4. Relation of specific conductance to dissolved-solids content in waters from the Sparta Sand in Arkansas, Louisiana, Mississippi, and Texas. electric logs was described by Turcan (I960).3 This analyses, were used to construct the dissolved-solids method was used to calculate the dissolved-solids con­ map (pi. 9).4 To avoid errors introduced by electrode tent of the water in the Sparta. The values thus spacing, calculations were not made for sands less than obtained, along with data from available chemical 15 feet thick. No values are shown for waters containing less than 200 ppm or more than 10,000 ppm dissolved 3 Turcan's method is based on the equation: solids. where * Contour intervals of 500, 1,000, 3,000, and 10,000 ppm are used on .F/=the field formation resistivity factor, the dissolved-solids map. These intervals were chosen on the bases of -R0=the resistivity read from the Ions-normal curve corrected to 77°F, the standards proposed by the U.S. Health Service (1962, p. 7-8) and JJK =the resistivity of the water at 77°F. the salinity classification given by Winslow (1956, p. 5). t-< t-< t-< t< E f Ir1 f 09 o O 0 0 B ° d d f 2 ! i I s C LMo-2..... LMo-1..... £ to S> % ! lo t-< £ Arkansas_. Mississippi.. Mississippi.. Louisiana... Louisiana... Louisiana... Louisiana... Louisiana.. Louisiana... QQ I;«_ i!cg_ a Arkansas.... £g p | P f! W o d u Sabine...__ Lincoln..... Lincoln__.. Claiborne..... Caldwell.._. & E. S 0 I i f | Rapides...... _Ouachita.. Ouachita._.. Morehouse.... Morehouse...... Drew. ___Desha.. 1§ p* § § f B.& ^ ^s

O M o ?£'!O DQ B- O a ^ L.Mc-J. | W| t* « " h» o /-> WtfM Villageof 5* W » Villageof zS w HS i Harold a^ g a g O p. ^ to CD w* Monroe. CityofWest Collinston. 2S » a ^ai" ^Id; Kennon. Cj _ p* |d te* C P oo ® S t| Choudrant. i g ? OQ O -i eQ S' 2*2* P **o H h-> H* CO 12-15-59 > 6-25-64 £ X 3-23-55 1 r ? £ V T w S 00 -1 I S f|| » H & 1 -J OS to S s I CO Oa r» 8 to to 8 -J 8 S s o g M CO g - o tO M CO i Silica (SiOs) -j * po & N p CO Total iron (Fe) 5 3 '° 3 k CO o o g K 8 g OS g too to=5 S 8 1 I ^ j_, t~* .* i ^ OS p H> N r* F* p Calcium (Ca) I "5. co o o - o -J Oi H> OO *>. o oo o to to OO CO *. CO I S Oi CO CO p Magnesium (Mg) to i-> to co J_ CO Oi to -J CO o to (6- o OS CO *. O it- s ,_, ,_, H» go­ 1"1 5 Sodium (Na) ~» g OS Oi -J Oi O M s 1 to s 1 s to e 8 5 OS i S ^ oo >^> to to s ^ H> [-> .* to CO Potassium (K) OS OO o OS «o -J o CO OS o Oi * o Oi j

H> §! £ to co Bicarbonate (HCOs) § ss 1 1 s i § § i to s § CO Oi Ol g i 5° po ~J en CO po o» Carbonate (COi) 0 0 o e o o o O o o o o o o O o o o s to IS CO Sulfate (SOO s : 13 CO to . P1 p= CTs oo oo o H> Oi -J V (6- OO 00 o oo 01 *>. CO 01 £ a l»- to co CO Chloride (Cl) 2.a" co po 1^- OS CO o & § O S° !* co _«.» 8P .* en OS 1 Oi O oo o OO o o 0 0 oo to a N 'H- ^ pi ^ p j Fluoride (F) a- CO OS t- CO 1*. *. Oi to *. *. u to H> OJ

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tO CO CO CO CO CO '& CO co to CO CO S & Oi Cn oo to s s s -j g s s s to -1 Percent sodium

H> Residue on ^ Oi CO CO to evaporation H Ol OS -4 CO H*. OI 01 oo i § § i S o B OJ g 1 Oi Cn i£ (fr. 01 (180° C) § gr £ Sum of & «f

-s to Specific conductance 5 S *. CO (microinhos at 25°C) i s co != 00 1 i i 1 OS 1 -j s I s IS 8 1 00 *-J oo *-j 7* 74 po P° p° 74 ;-J po p 74 p° po po 00 00 PH Oi 00 J OS OS to o eo oo 09 2 OS co to o o ^- jnoao xaoaivio ani, &o STV HYDROLOGIC SIGNIFICANCE OF THE LITHOFACIES OF THE SPARTA SAND A13

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SELECTED BIBLIOGRAPHY Bedinger, M. S., and Reed, J. E., 1961, Geology and ground-water resources of Desha and Lincoln Counties, Arkansas: Arkan­ (Annotated for publications containing specific information sas Geol. and Conserv. Gornm. Water Resources Circ. 6, on the Sparta Sand) 129 p. Albin, D. R., 1964, Geology and ground-water resources of Briefly discusses geology and hydrology, pumping test re­ Bradley, Calhoun, and Ouachita Counties, Arkansas: U.S. sults, public water supplies, and chemical quality. Tabulates well Geol. Survey Water-Supply Paper 1779-G, 32 p. descriptions, water levels and chemical analyses. Includes Discusses depositional history, lithology, thickness, water- geologic sections. yielding characteristics, water quality, and potential for devel­ Bornhauser, Max, 1947, Marine sedimentary cycles of Tertiary opment. Includes cross sections, geologic map, and hydrographs in Mississippi embayrnent and central Gulf Coast area: Am. and indicates approximate depths to base of fresh water. Tab­ Assoc. Petroleum Geologists Bull., v. 31, no. 4, p. 698-712. ulates maximum, minimum, and most representative concentra­ Discusses application of rhythmic (cyclical) deposition to tions of chemical components of 34 samples analyzed. Sparta and other Tertiary formations. Includes isopach map of Alexander, W. H., Jr., Myers, B. N., and Dale, O. C., 1964, Re- Cane River-Sparta interval. connaissance investigation of the ground-water resources 1950, Oil and gas accumulation controlled by sedimen­ of the Guadalupe, San Antonio, and Nueces River basins, tary facies in Eocene Wilcox to Cockfield formations, Loui­ Texas: Texas Water Cornm. Bull. 6409, 106 p. siana Gulf Coast: Am. Assoc. Petroleum Geologists Bull., Anders, R. B., 1957, Ground-water geology of Wilson County, v. 34, no. 9, p. 1887-1896. Texas: Texas Board of Water Engineers Bull. 5710, 62 p. Recognizes marine phases of Sparta downdip. Indicates strati- Briefly discusses geology, water characteristics, and poten­ graphic relations. tial for development. Includes geologic map and cross sections. Bredehoeft, J. D., 1964, Variation of permeability in the Ten- Tabulates chemical analyses, well descriptions, and water levels. sleep Sandstone in the Big Horn Basin, Wyoming, as in­ 1960, Ground-water geology of Karnes County, Texas: terpreted from core analyses and geophysical logs: U.S. Texas Board of Water Engineers Bull. 6007, 107 p. Geol. Survey Prof. Paper 501-D, p. D166-D170. Briefly describes geology. Includes geological cross sections. Brown, G. F., 1947, Geology and artesian water of the alluvial Anders, R. B., and Baker, E. T., Jr., 1961, Ground-water geology plain in northwestern Mississippi: Mississippi Geol. Survey of Live Oak County, Texas: Texas Board of Water Engi­ Bull. 65, 424 p. neers Bull. 6105, 119 p. Discusses geology and hydrology of Kosciusko (Sparta) Sand. Briefly describes geology. Includes geologic sections and maps structure of base. Tabu­ lates screen analyses and laboratory coefficients of permeability, Andersen, H. V., 1960, Geology of Sabine Parish: Louisiana chemical analyses, descriptions of wells and water levels, and Geol. Survey. Geol. Bull. 34, 164 p. sample and drillers' logs. Discusses geology and stratigraphic relations. Describes fos- Callahan, J. A., 1963, Ground-water resources in Yazoo County, siliferous and glauconitic estuarine and lagoonal beds in upper Mississippi: Mississippi Board Water Commissioners Bull. and lower parts. Includes geologic map and geologic section. 63-5, 42 p. Baker, B. B., Dillard, J. W., Souders, V. L., and Peckham, R. C., Describes geology and discusses hydrology. Includes chemi­ 1963, Reconnaissance investigation of the ground-water re­ cal analyses and geologic section. sources of the Sabine River basin, Texas: Texas Water Cornrn. Bull. 6307, 57 p. Chawner, W. D., 1936, Geology of Catahoula and Concordia Parishes: Louisiana Dept. Conserv. Geol. Bull. 9, 232 p. Describes geology and quality and availability of water. In­ cludes geologic cross sections and map. Describes geology and mentions occurrence of marine fossils. Cooke, C. W., 1925, Correlation of the Eocene formations in Baker, B. B., Peckham, R. C., Dillard, J. W., and Souders, V. L., Mississippi and Alabama: U.S. Geol. Survey Prof. Paper 1963, Reconnaissance investigation of the ground-water 140-E, p. 133-135. resources of the Neches River basin, Texas: Texas Water Comrn. Bull. 6308, 67 p. Briefly describes Sparta Sand and shows regional correlations. Briefly describes geology. Discusses hydrology, including wa­ Cooke, C. W., Gardner, J. A., and Woodring, W. P., 1943, Correla­ ter movement, recharge, discharge, water levels, water-bearing tion of the Cenozoic formations of the Atlantic and Gulf characteristics, chemical quality, utilization, development and Coastal plain and the Caribbean region: Geol. Soc. America availability. Tabulates chemical analyses and purnpage. In­ Bull., v. 54, no. 11, p. 1713-1723. cludes geologic map, geologic cross section, and isopachous map Includes correlation chart showing Sparta. and indicates altitude and depth of top Sparta aquifer. Cronin, J. G., Follett, C. R., Shafer, G. H., and Rettman, P. L., Baker, R. C., Hewitt, F. A., and Billingsley, G. A., 1948, Ground- 1963, Reconnaissance investigation of the ground-water re­ water resources of the El Dorado area, Union County, Ar­ sources of the Brazos River basin, Texas: Texas Water kansas: Arkansas Univ. Bur. Research, Research Ser. 14; Comm. Bull. 6310,152 p. Arkansas Univ. Bull., v. 42, no. 12, 39 p. Briefly describes Sparta Sand. Discusses water movement, Describes geology. Discusses history of ground-water devel­ recharge, discharge, utilization of water, present develop­ opment, water levels, pumping tests, quality of water, and safe ment of aquifer, water levels, chemical quality, availability of yield. Includes chemical analyses. water, potential development of aquifer, and some problems of A16 GEOHYDROLOGY OF THE CLAIBORN GROUP water from Sparta. Tabulates chemical analyses and pumpage. Klein, Howard, Baker, R. C., and Billingsley, G. A., 1950, Includes geologic sections and geologic map. Ground-water resources of Jefferson County, Arkansas: Gushing, B. M., Boswell, B. H, and Hosman, R. L., 1964, Gen­ Arkansas Univ. Inst. Sci. and Technology, Research Ser. eral geology of the Mississippi Bmbayment: U.S. Geol. 19, 44 p. Survey Prof. Paper 448-B, 28 p. Discusses geology and hydrology. Briefly describes geology. Indicates configuration of top of LeGrand, H. B., 1964, Hydrogeologic framework of the Gulf and Sparta. Atlantic Coastal Plain: Southeastern Geology, v. 5, no. 4, DeVries, D. A., and others, 1963, Jasper County mineral re­ p. 177-194. sources: Mississippi Geol. Bcon. and Topog. Survey Bull. Lonsdale, J. T., 1935, Geology and ground-water resources of 95,101 p. Atascosa and Frio Counties, Texas: U.S. Geol. Survey Describes Kosciusko (Sparta) Sand. Briefly discusses hydrol­ Water-Supply Paper 676,90 p. ogy. Tabulates descriptions of wells, water levels, and chemical Differentiates Sparta and includes it in Cook Mountain and analyses. post-Bigford. Includes chemical analyses, and descriptions of Bllisor, A. C., 1929, Correlation of the Claiborne of east Texas wells. with the Claiborne of Louisiana: Am. Assoc. Petroleum Maher, J. C., and Jones, P. H., 1945, Ground-water and geologic Geologists Bull., v. 13, no. 10, p. 1335-1346. structure of Natchitoches area, Louisiana: Am. Assoc. Pe­ Briefly describes Sparta. Correlates various formations of troleum Geologists Bull., v. 29, no. 1, p. 40-41. Claiborne. Indicates thickness variations. Describes geology and hydrology. Includes geologic sections. Msk, H. N., 1944, Geological investigation of the alluvial valley Martin, J. L., Hough, L. W., Raggio, D. L., and Sandberg, A. B., of the lower Mississippi River: Vicksburg, Miss., U.S. Dept. 1954, Geology of Webster Parish: Louisiana Geol. Survey, Army, Mississippi River Comm., 78 p. Geol. Bull. 29,252 p. Harvey, B. J., Callahan, J. A., and Wasson, B. B., 1961. Ground- Describes geology. Includes geologic map and sections. water resources of Hinds, Madison, and Rankin Counties, Meinzer, O. B., 1923, The occurrence of ground water in the Mississippi, Part II, Basic data: Mississippi Board Water United States: U.S. Geol. Survey Water-Supply Paper 489, Commissioners Bull. 61-2, 146 p. 321 p. Describes geology. Tabulates descriptions of wells and water Meinzer, O. B., and Wenzel, L. K., 1942, Movement of ground levels, data on municipal supplies, logs of wells, and chemical water and its relation to head, permeability and storage, in analyses. Physics of the Earth, pt. EX, Hydrology: New York, 1964, Ground-water resources of Hinds, Madison, and McGraw^HiU Book Co., p. 444-477. Rankin Counties, Mississippi: Missisippi Board Water Com­ Moody, C. L., 1931, Tertiary history of region of Sabine Uplift, missioners Bull. 64-1, 38 p. Louisiana: Am. Assoc. Petroleum Geologists Bull., v. 15, Describes geology. Discusses water levels and movement, well no. 5, p. 531-551. yields and aquifer characteristics, water quality, and develop­ Discusses stratigraphic relations, the strand line, and geo­ ment of water supplies. Tabulates records of municipal water logic history. supplies, descriptions of wells, chemical analyses, and results of Murray, G. B., 1961, Geology of the Atlantic and Gulf Coastal pumping tests. province of North America: New York, Harper & Brothers, Hem, J. D., 1959, Study and interpretation of the chemical 692 p. characteristics of natural water: U.S. Geol. Survey Water- Discusses regional correlations and relationships. Indicates Supply Paper 1473, 269 p. structure. Contains excellent bibliography. Hewitt, F. A., Baker, R. C., and Billingsley, G. A., Ground-water Onellion, F. B., 1956, Geology and ground-water resources of resources of Ashley County, Arkansas: Arkansas Univ. Inst. Drew County, Arkansas: Arkansas Geol. and Conserv. Sci. Technology, Research Ser. no. 16, 35 p. Comm. Water Resources Circ. 4,43 p. Describes geology and possible water supply potential. In­ Describes geology. Discusses aquifer test data, utilization of cludes geologic sections showing fresh water in Sparta. water, and chemical constituents and quality. Tabulates well Huner, J. H., Jr., 1939, Geology of Caldwell and Winn Parishes: descriptions, water levels and chemical analyses. Includes geo­ Louisiana Dept. Conserv. Geol. Bull. 15, 356 p. logic sections. Describes geology in detail, including mode of deposition. Onellion, F. B., and Criner, J. H, Jr., 1955, Ground-water re­ Mentions calcareous shales and shell fragments. Includes geo­ sources of Chicot County, Arkansas: Arkansas Geol. and logic map and sections. Conserv. Comm. Water Resources Circ. 3,32 p. Jones, P. H., and Holmes, C. N., 1947, Ground-water conditions Briefly describes Sparta. in the Monroe area, Louisiana: Louisiana Geol. Survey Bull. Page, L. V., and May, H. G., 1964, Water resources of Bossier 24, 47 p. and Caddo Parishes, Louisiana: Louisiana Geol. Survey and Describes geology and some hydraulic characteristics. Dis­ Dept Public Works Water Resources Bull. 5,105 p. cusses water resources, hydrology, and quality. Tabulates chem­ Briefly describes Sparta. Discusses water-bearing character­ ical analyses, mechanical analyses, and results of drill stem istics, quality, and water-supply potential. Tabulates chemical tests. Includes geologic sections. analyses, well descriptions, and water levels. HYDROLOGIC SIGNIFICANCE OF THE LITHOFACIES OF THE SPARTA SAND A17

Page, L. V., and Newcome, Roy, Jr., 1963, Water resources of Sundstrom, R. W., and Follett, C. R., 1950, Ground-water re­ Sabine Parish, Louisiana: Louisiana Geol. Survey and Dept. sources of Atascosa County, Texas: U.S. Geol. Survey Water- Public Works Water Resources Bull. 3,146 p. Supply Paper 1079-C, p. 107-153. Briefly describes Sparta. Discusses hydrology, water resources Does not differentiate Sparta, but it is probably included in and quality. Tabulates descriptions of wells, water levels and Cook Mountain aquifers. chemical analyses. Tait, D. B., Baker, R. C., and Billingsley, G. A., 1953, The Parks, W. S., Moore, W. H., McCutcheon, T. E., and Wasson, ground-water resources of Columbia County Arkansas a B. E., 1963, Attala County mineral resources: Mississippi reconnaissance: U.S. Geol. Survey Circ. 241, 25 p. Geol. Economic and Topographic Survey Bull. 99, 192 p. Briefly describes Sparta. Tabulates records of wells, water Describes geology in detail. Includes geologic map and section. levels, and chemical analyses. Discusses hydrology. Turcan, A. N., Jr., 1960, Estimating water quality from elec­ Peckham, R. C., Souders, V. L., Dillard, J. W., and Baker, B. B., trical logs: U.S. Geol. Survey Prof. Paper 450-C, p. C135- 1963, Reconnaissance investigation of the ground-water re­ C136. sources of the Trinity River basin, Texas: Texas Water U.S. Public Health Service, 1962, Drinking water standards: Comm. Bull. 6309,110 p. U.S. Dept. Health, Education, and Welfare, Public Health Describes geology in fair detail. Discusses water movement, Service Pub. 956,61 p. recharge, discharge, water levels, water-bearing characteristics, Vaughn, T. W., 1895, The stratigraphy of northwestern Louisi­ chemical quality, and utilization and availability of water. Tab­ ana : Am. Geologist, v. 15, p. 205-229. ulates chemical analyses and pumpage data. Shows aerial geol­ Proposes name "Sparta." ogy. Includes geologic section. , 1896, A brief contribution to the geology and paleontol­ Pettijohn, F. J., 1957, Sedimentary rocks: New York, Harper ogy of northwestern Louisiana: U.S. Geol. Survey Bull. 142, Bros., 718 p., 2d ed. 65 p. Poole, J. L., 1961, Ground-water resources of East Carroll and Describes and names Sparta Sand. West Carroll Parishes, Louisiana: Baton Rouge, Louisiana Wang, K. K., 1952, Geology of Ouachita Parish: Louisiana Geol. Dept. Public Works, 174 p. Survey. Geol. Bull. 28,126 p. Discusses classification, cyclical sedimentation, stratigraphy, Describes Sparta in detail. and water-supply potential, p. 59-61. Welch, R. N., 1942, Geology of Vernon Parish: Louisiana Dept Rollo, J. R., 1960, Ground water in Louisiana: Louisiana Geol. Conserv. Geol. Survey Bull. 22, 90 p. Survey and Dept. Public Works Water Resources Bull. 1, Shows Sparta on geologic sections. 84 p. Wendlandt, E. A., and Knebel, G. M., 1929, Lower Claiborne of Briefly discusses geology and hydrology. east Texas, with special reference to Mount Sylvan dome and salt movements: Am. Assoc. Petroleum Geologists Bull., Sellards, E. H., Adkins, W. S., and Plummer, F. B., 1932, The v. 13, no. 10, p. 1347-1375. geology of Texas, Volume I. Stratigraphy: Texas Univ. Describes Sparta Sand and Tyler Greensand in Sparta. Con­ Bull. 3232, 1007 p. siders Sparta Sand a member of Cook Mountain Formation. Describes geology in fair detail. White, W. N., Sayre, A. N., and Heuser, J. F., 1941, Geology and Spooner, W. C., 1926, Interior salt domes of Louisiana: Am. ground-water resources of the Lufkin area, Texas: U.S. Assoc. Petroleum Geologists Bull., v. 10, no. 3, p. 217-292. Geol. Survey Water-Supply Paper 849-A, p. 1-58. Describes and redefines Sparta Sand and discusses mode of Briefly describes Sparta. Discusses availability and quality of deposition. water. Includes chemical analyses. Stenzel, H. B., 1938, The geology of Leon County, Texas: Texas Winslow, A. G., 1950, Geology and ground-water resources of Walker County, Texas: Texas Board of Water Engineers Univ. Pub. 3818,295 p. Bull. 5002, 48 p. Stenzel, H. B., Krause, E. K., and Twining, J. T., 1957, Pelocy- Briefly describes Sparta. Includes geologic sections. poda from the type locality of the Stone City beds (middle Winslow, A. G., and Kister, L. R., 1956, Saline-water resources Eocene) of Texas: Texas Univ. Pub. 5704, p. 18-35. of Texas: U.S. Geol. Survey Water-Supply Paper 1365,105 p. Discusses relation of fossiliferous Stone City beds to Sparta Discusses Sparta. Includes saline water classification and Sand. chemical analyses.

U.S. GOVERNMENT PRINTING OFFICE: 1968