SALT OONIAMINATION OF THE BRAZOS RIVER FROM 'FHE DOVE CREEK AND CROTON CREEK AREAS, TEXAS Them for he Demo. 9! M. S. MICHPGAN' STATE UNIVERSITY Lesiio Gian MCMEHSW 1957 JHESI: SUPPLEW "a 5' 33; BM“ 0F BOOK LIBRARY . University 3LT CITAIIKATI 7! P'", “Q" ”.5"? 1 3,! “-3 “"3 mu...‘ . L Leslie 3. SALT CONTAMINATION OF THE BRAZOS RIVER FROM THE DOVE CREEK AND CROTON CREEK AREAS, TEXAS By Leslie Glen McMillion A.THESIS Submitted to thewCollege of Agriculture Michigan State University of.Agriculture and Applied Science in partial fulfillment of the requirements for the degree of MASTER OF SCIENCE Department of Resource Development 1 9 5 7 Approved 'flflW’Jc 7 fl I" 7‘5”“, ’ g, 7..“ ".- if . Liza? W1. : .m x J “E” $.33“: Lining]: L. I CONTENTS EJBACROCBx—xcz\ Page Introduction - - - ----- - ........... 1 Previous work done on the salt problem 9 Scope of this investigation 10 Acknowledgements 11 General description of detailed area - ------- 13 I Climate and soils ----------------- 15 Stratigraph - - - ----------------- 1'7 Permian deposition 1'? Correlation 19 Permian system 20 Guadalupe series ifll Reno (Pease River) group 23 'Ihitehorse group 24 Ochoa series 26 Quaternary deposits 26 Salt producing areas ---------------- 28 Dove Creek area i 28 Cretan Creek area 35 Geomorphology 37 Origin of Dove Creek Flat 39 Origin of Salt Flats of Hayrick Creek 45 Salt Producing; (h'igin of 5‘. Geologic se’. Eyirology . . “mm: a Source of as Source Of ea Structure ktesim 335868th me thc "tar . . _ “auction 01 C ONTENTS Salt Producing areas - continued Origin of Short Croton and Hot Springs Flats Geologic sections in the salt producing areas Hydrology - - - - ---------------- Topography and the water table Source of salt water in Croton Creek area Source of salt water in Dove Creek area Structure Artesian system of the Childress gypsum Suggested methods for decreasing amount of salt 'ator ---------------- ...... Reduction of salt in Dove Creek area Reduction of salt in Groton Creek area Suggestions for future studies - - - - - - - - - .. Eastern extent of salt beds in Permian deposits Bibliography Page 44 52 58 58 60 65 68 '72 82 82 89 93 95 99 Figure 1. 2. 5. 4. 5. 6. 7. 8. 9. 10. 11. 12. 13. 14. 15. I L L U S T R A T I O N S Page Average annual rainfall for Texas as of January 1, 1956 - - - - - - - - - - - 5 Net reservoir evaporation loss in the Brazos River watershed and in Texas - - 4 Brazos River'watershed with average annual run-off in inches for 50-year period, 1924-1955, inclusive - - - - - - 5 Brazos River watershed with average annual run-off in inches for 4-year period, 1950-55, inclusive - - - - - - - 6 Index map showing location of detailed area in Texas - - - ---------- 12 Outcrop map of rocks from Permian through Cretaceous - - --------- - - - - 13 Correlation of Permian rocks of detailed area with standard reference sections - - 21 ‘Western part of.Abilene Geological Society cross section, Scurry Co. to Parker 00., Texas, 1949 - - - - - - - -------- 22 View of Dove Creek area taken from a point one mile south of Dove Creek Flat - - - - 50 Steep bluff on Hayrick Creek showing'El Reno clay below the Childress gypsum- - - 30 Detail of the clay shown in figure 10 - - 51 Same clay, as in figure 11, exposed near mouth of Dove Creek Flat - - - - - - - - 51 Low bluffs or scarp around upper part of Dove Creek Flat - - - - - - - ------ 42 Detail of Childress gypsum shown in fig- ”.13-----------------42 Talus of small dry wash entering the Lower Salt Flat of Hayrick Creek - - - - 45 Figure 16. 17. 18. 19. 21 22. 25. 24. 25. 26. 27. ILLUSTRATIONS Page One of several knolls in Lower Salt Flat of Hayrick Creek --------- View of Croton Creek area taken from a point about 5/4 mile southwest of Short Croton Fiat - - - - - - ----- Closer view of canyon at left side of figur°17------------——— llO-foot bluff on southwest side of Short Croton Flat - - - - - - ........ Detail of salt crust in figure 19 - - - Hard, resistant, 6 to 8-inch clayey layer formed by ground water in the floor of the southwest corner of Short Croton Flat -------------- Salt water "spring” about 12 feet from hole shown in figure 21 ----- Rough, salt-gypsum crust as is typical in Short Croton and Hot Springs Flats - Small cone-shaped pits occur between main drainage courses in Short Croton Flat --- -------------- Vertical section showing the ground- water hydrology of the Croton Creek ”ea------- -------- -- Determination of the eastern extent of salt deposits in Permian rocks - - - - Generalized diagram showing the way that an artesian system could develop up the dip in the Childress anhydrite- mam-------—-—---—-- Cavern about ten feet high in the Child- ress gypsum at a place several yards upstream from the proposed dam site on Dove Creek Flat - - - - - - - - - - - - 45 48 48 49 49 50 51 51 63 71 78 84 Figure 29. Plate Plate Plate Plate Plate Table 50. 1. 2. 5. 4. 5. ILLUSTRATIONS Page Salt crust forming in Dove Creek Flat--—-------------- 84 Map showing location of oil-test holes drilled with cable-tool equip- ment in and near the detailed area - - 96 land map of parts of Stonewall, Kent, Dickens, and King Counties, Texas show- ing locations of water wells, deep oil tests, exploration holes, measured geo- logic sections, and outcrop of base of Chi 1dres s gypsum . Reconnaissance topographic map of parts of Stonewall, Kent, Dickens, and King Counties, Texas. Reconnaissance map of the water table in parts of Stonewall, Kent, Dickens, and King Counties, Texas. Structure map on the top of the Childress gypsum in parts of Stonewall, Kent, Dickens, and King Counties, Texas. Structure map on the top of the Upper Eskota gypsum in parts of Stonewall, Kent, Dickens, and King Counties, Texas. (.All plates inside pocket of back cover ) 1. Page Records of wells in parts of Stonewall, Kent, Dickens, and King Counties, Texas - 104 Table 2. 5. 4. ILLUSTRATIONS Page Partial record of oil-test holes drilled with cable-tool equipment in and near the detailed area - - - - - - 113 Record of exploration holes showing elevations of surface and tops of marker beds used in report - - - - - - - 115 Drillers' logs of cable-tool holes Dunberfl 88, 93’ and 98 --------- 131 ABSTRACT SALT CONTAMINATION OF THE BRAZOS RIVER FROM THE DOVE CREEK AND CROI‘ON CREEK AREAS, TEXAS By Leslie Glen McMillion An area of about 545 square miles in northwest Texas contributes unusually large quantities of salt to the Brazos River. The salt damages craps which are irrigated with water from the river and limits the uses of the water by industries and municipalities. The users greatly de- sire to reduce the quantity of salt contributed by this area, and the Brazos River Authority plans to spend $7,500,000 for this purpose. The writer studied the area for four months to deter- mine the source or sources of salt water and thus be able to suggest methods for alleviating the situation and to suggest future plans of study. The detailed area is conveniently divided into the Croton Creek area, western part, and the Dove Creek area, eastern part. Spectacular salt flats occur in each of these areas. The rocks cropping out are of Permian age and dip regularly west 25 feet per mile. The Childress gypsum is the most prominent marker bed; below its base lies clay of El Reno group and above it is sand of White- horse group. A thick salt section belonging to the Seven Rivers formation, Whitehorse group, occurs in the shallow subsurface. In the Croton Creek area, unconfined ground Leslie Glen McMillion Abstract, Continued water moves downward through some of these salt beds and issues at the surface as widespread salt-water seepage. The situation is intensified by land conservation practices which cause increased recharge to the water table of the nearby plain, thus increasing the amount of salt water dis- charged. Recently irrigation by ground water has been started in this area and the local interest in favor of such irriga- tion is strong. An intensive irrigation program here would lower the water table and could possibly step all discharge of salt water into the Croton Creek drainage system. Artesian salt water occurs in the Dove Creek area. By an elimination process, the artesian pressure is inferred to be developed in a cavernous system up the dip in the Childress gypsum, which is anhydrite in subsurface. The pressure is produced by a distal water table much higher in elevation than the elevation of the salt water discharge in Dove Creek. The salt water is forced out of the Childress is the shallow subsurface where anhydrite is changing to gypsum, moves into the underlying El Reno clay} and seeps to the surface. Five methods of disposal were suggested, however, much more de- tailed research is needed to decide which one is most ap- prepriate. A coring program to determine the character- istics and pressure heads of the Childress artesian system is strongly urged. The program for measuring the amount of salt carried by streams of the Brazos River should be expanded to determine if any other areas are large producers of salt, and if so found, studies of these areas should be made. INTRODUCTION The Brazos River watershed is the largest watershed within the State of Texas. Its extension is from eastern New Mexico across Texas in a southeasterly direction to the Gulf of Mexico. Overall length of the watershed is 640 miles and the maximum width is 120 miles; its total area is about 44,670 square miles - 2,675 square miles in New Mexico and the remainder in Texas. The distance along the river channel from eastern New Mexico to the Gulf of Mexico is 1,210 miles. This watershed is in three physiographic provinces of the United States (Finneman, 1931). These provinces are the Great Plains, Central Lowlands and Coastal Plain. The Great Plains province, being divided by an extension of the Central Lowlands, occupies two separate areas in the watershed. The first of these areas is the High Plains. The other is the Central Great Plains area which is bounded on the northwest by low escarpments extending across the watershed near Mineral'Wells, Texas, and on the southeast by a series of small escarpments near‘Waco, Texas. The Central Lowlands province of the watershed is the area be- tween the two Great Plains areas. The Coastal Plain oc- cupies the part of the watershed between the Central Great Plains area and the Gulf of Mexico. The High Plains area of the watershed has little re- lief. It declines gently to the southeast with land eleva- ‘tions ranging from about 4,500 feet along the northwestern (THE [{DE. l‘rlll {Mum I IONIIMAI .I _I_T.55 I. . iwfl' “00.! It‘ll! nv‘al'esg W. 33?? iii: “0‘.- I ."IMIDA 4.23 “a.” “IV-o ‘ ems-«n l0.83 "WM '0 I‘ .32.: I \1, E In ' mull IImvnI I 02 I I Jul/“.4353” ?‘4 (9 £25“ I { I1 I s I was nu u H) II -n I W nu~ 11:10:. - 1 "n“ Iago-cu I may 30 I 5” 40M 13 '47 4:) I un.’ I532. II' "as“. 1&9; mun “W . "V ”n ubuulv“ u: snout n .m- 4 '6 "(In as ""10 I“ v 1553“” ‘m- -- emmqo- 20 ....-. IIISIEMI’ III" ”I.“ WII‘I'IEII"? . Main new ' % '”2 I .'~‘ IE8 04 : ' . u'z' ‘ I I hm 'Iusnvu "Inavz can“ and Int-”Wan I'll u ' Ivvnotuumwnb IOU”. I/ JI a." ”‘1‘!“ 'I“ IN“'"'" '4‘" "sun 0 |'[ I3‘03 A" an" M" "nub ' mutual I . 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'1. ’4. ._~.I‘ E" 157:.“ I J "II “II ::’:no- I.II‘ ma£aI .- ; .uwnun IIN flurry uni ,___ . - ,. 1.0”" f ""35 2/“"" . . 2 ' an in ' ‘ . ‘ 9 I ‘ I . I " as am {0 gig—ZQ‘, I ‘. ‘4 22.76 OI . fl, 9qu [4'4 2733r‘tm1yhlgakfl ‘6;." 5 ' . . . - . us "mu :9 249 gm on}. f . - A ..I )I I I I'IJ . 4,. .587 It; I. ’39) nus u I‘ . ‘. ' ‘. . . fl . ’ "Tu-...: ' I40\. 2.”... "18%"; .2315; \ .I ' ' .\I’\ ..un chm, I '_ A. 2‘ [MB ." .10": 52 52 . h .2 \ -\ nmu I" "' g9;)’% Inqu on u \%.'l' wlsr 2" sails! ”W“ .5: n I %.INA;fiiI flsrd,‘ Nuz‘iu} .II. at 4;.I\:lull Riv“- ‘ I 7 I I s an I I b a I" . ulnwuo .) ‘4 _ IvI .- _ . 4 3" 55-55 0.,OIIO W.,'“& I 379%. ‘4)» I. ' nun" . .uuu “I 213 7. 4'" nu r . . V. 43?; I836 """' ‘ ,- ,' M 09 "‘Inol , _ o‘fiu'. I L' .' ?l In». A 4:0,! \ / ham, 2&7. , _ '_ :3 5...”, I I’ll... I EXPLANATION I656 'Avwooe annual Ior sIaIIon ”.35 -Annuol Ior I955 lesion of I955 flours Indicates Incomuele ”cords Io' that year. STATE OF TEXAS BOARD OF WATER ENGINEERS AUSTIN, TEXAS AVERAGE ANNUAL RAINFALL AS OF JANUARY I, I956 AUGUST. I050 I '1 1;: Figure 1. Average annual rainfall for Texas as of January 1, 1956. It mug? «‘7 ' CIMARRON NAuIIono’ L"IC0I| '1 60 NUTCNIN’ON +'—— BECKHA 'NOSWOIVN r.__. \ 4’ , l \\’,!o I CURTAIN .1 ‘7 fl sxA,I(LIouu V‘kLl'k 'TIPSS ""“ ._. , \____I_. -.— . I EASVIHAW [941:1 ' \ NC CULLOCN \_/= 906lN7‘50 ' / A NRA / / uw‘usok “H" /nuuos . / I I . . . . \,a- /L \juu . . ._ .x.. J‘ . .. , ‘ '1 . -- \ VH‘V‘SVR._E( E \‘\“ I /. 1,2» .- \\ —L _J... _' _ . . ' ' I \ \f/,IA‘.H '4',‘ ‘ r - . \I suvgoir ‘ \ \q‘ ’ "I uo~lco Ln 8 SYIO I JgIIIZ'50“ I HAVIRICI NET RESERVOIR. EVAPORATIONLOSS 'IN TEXAS ' AVERAGE FOR PERDD ININCHES |95|—1955 ROBERT LOWRY AUSTIN,TEXAS CONSULTING ENGINEER MAY, I956 \ :1" ' P s .r .'3 , I J - ~11 R a to" ' . I, -'.' f' ’ , .q ‘3. - . fr I ..f..' _) I i, V ' ' f 1 ‘ I - ' I 5- 2 .sf. '. Figure 2. Net reservoir 4 evaporation loss in the h . dg' Brazos River watershed e , 5.. .‘F‘3_[ and in Texas. .; . ;5;1 ' . {0-1 It cmAuRou no ,I: A'vta . i kl’lcoll ‘ IfiIé.l \ A I _ _ TEXOMA BRYAN AAAAAA ’ VIQV "Slll nnnnn IIIII —L1 COLIIAI SABINE cu;.;.,°./ /. ./‘ JI" on”. uuuuu ...... ICIDLLII '~" CAI OUVlt l ’nulclt "Lflt'l\\ . I T. ,f ‘ n r E c IO 0 IO 10 IO ‘0 56 I0 70 MILES STATE OF TEXAS BOARD OF WATER ENGINEERS AUSTIN, TEXAS STORAGE RESERVOIRS ON TEXAS RIVERS OCTOBER, I954 Figure 5. Brazos River watershed with average annual run-off in inches for 50-year period, 1924-1953, inclusive. VENUSTIANO AREA a“, .If ”I'nsou I I I MURRAYI [MIARV‘AAALV T ....... 1 o\ I I I: ' YII‘L‘ I I: . ‘2 LIIAVON II . I. I \ii‘ I I, l r I I I If. I AOL—E WITHIN _ .i'I ’ . .1 I _ I I m I I II ‘I I I Z I I I I I <1 J I .I I r I I x T “I ' Aw I I L: [I l 5 < dARzA—LITTuI ELM / MI I I. ..... . | l ..‘n .L.. , I‘I .' H ' I t.’ ", I V,‘ I ,T I v‘ Hr. Kn ‘ A: I . \‘ y\ > I V l ,’ / w J I I x / I I J 7 ‘rr 3 . . I ’I I I I ~’ . . .. 1 05 I ‘7 ~\ .2. \ \ '0. I: u l I v ‘ " ' ' . I I 2~ ‘- , SIA‘II “IIjifimTo' All ‘ADDICKS '{ /I a. r . V,\, -// ,. / I .‘r / / I I”\I I I u , j-‘ I I’ ) I, I .. . I » ”I I ‘MA ’3 ’ . , . ' fly I I A z I .' I 0 0 I )0 ‘0: 50 ‘0 O mus :3 / STATE OF TEXAS BOARD OF WATER ENGINEERS AUSTIN, TEXAS J STORAGE RESERVOIRS ‘7 ON TEXAS RIVERS A Ii '1“ Al Ii; %1 fiw OCTOBER, |:54 l- _BY'JPD Figure 4. Brazos River watershed with annual run-off in inches for 4-year 1950- -1953, inclusive. average period, 'Jl' \ above normal rainfall and consequently, the dam soon filled with water. The Brazos River Authority has long realized that the water of the headwater streams of the Brazos River is high in mineral content, especially in sodium chloride (NaCl) and in calcium sulfate (CaSo4). ‘When run-off is large, as in 1941, the minerals are so diluted that the large quan- tity present is not easily noticed. However, with small run-off and with reduction of bodies of water in reservoirs by evaporation, the mineral content or dissolved solids increases in parts per unit of water and the uses of the water are controlled by the concentration of the mineral content. Sodium chloride or common salt is extremely injuri- ous to vegetation. The Brazos River watershed and much of the Southwestern United States endured one of the worst droughts in recorded history during the period 1950 through 1956. The dissolved solids in the Brazos River at the Possum Kingdom Dam increased from a few hundred parts per million in 1941 to an average of 1,200 parts per million in the water year October, 1955 to September, 1954. Dur- ing 1941 to 1952, the Possum.Kingdom water contained chloride in quantities less than 100 parts per million; however, since 1952 the water has contained chloride as high as 700 or 800 parts per million. Records of chemical analyses of the river at the Possum Kingdom Dam are avail- able for the period from January, 1942 to September, 1954. On the next page is a partial record of these chemical CH ooH.m oom.H owe mew mew meo.a omeno>a eopnwaos onH.m osm.a one pom mam flea ------onua .peom omo.m oom.H one mam new mom -------H9-H .wse oom.a omH.H oHe 0mm mom ewe ------uanua base oma.~ oeH.H one one are moe.a ------uon-a ease omo.m 00H.H owe one Hem ane.m ------uuanua has omo.m on.H ope Hem «am new ------uon-H .ne4 con.m oom.a can Ham can emu -------Hn-H .psz era.» oms.a one «mo nee e.mn -------ma-m .nom onm.m ome.a who Hem son mmn umm-om .mua .nmm omm.m con.H com mom «an new uemma .Hnua .cwe ono.m omH.H nee mam mmm men ------uan-a .ooo ooo.m OHN.H one new new mom ------aonua .>oz omn.m omn.H one com own one -nmma .HnIH .poo Aoomm as monsouo meadow “Hov Aeomv Amy hazy Annoy I25 oofiduofiv UmPHOmmHQ 00am" 09w“ 845m ESHO omnm£OMHQ GOHUOOHHOO IGOO Odhaommm Hanan. IOHSD IHfim Imdpom low EGGS .Ho endow emma monsopaom on mama homepoo sash mops: .GOHHHHB sea magma ca .momhasoo Hwofiaono ac osooon acapnwm .waapsnfinpnoonooq hand .nona ma moHHE masses owm.m Scan: Mo .haopwaaxonams .moHHE cheddm omn.mmll.son4 owdqawnm .Opqflm oaam neon qoapwpm mud nwmw Bonn escapees moHHE 0N was .huqzoo oanm oawm .mnoneaw Mo pmoknusom moaaa n.HH .xoonu wnapoa scum Homepage modes o.m .Aopdm moudam :0 sec BoHon haopdaooEEHul.noapaooq magma .mmomame mama 24o sooesz zpmmom as mm>Hm momamm analyses from October, 1952, to September, 1954. Conservation programs on the farm and range lands and increased water useage in the drainage areas have also re- duced the amount of run-off. Some of the practices under the conservation programs are as follows: Contour farming Cover cropping Crop residue management Stubble mulching Terracing Pond construction Irrigation with ground water is extensive in several coun- ties between the salt contributing area and the Possum Kingdom Reservoir. This ground water used in irrigation must be replaced by surface recharge before discharge to streams takes place; thus, run-off is reduced. If the rain- fall returns to normal in this area, the run-off will only be about 57 per cent of the run-off before these conserva- tion practices and water uses were begun (Lowry, 1955). Therefore, it is paramount that a program be developed to reduce the salt content of the headwaters of the Brazos River. Previous york done on the Salt Problem A program was begun in 1954 to study the sources of salt water entering the upper reaches of the river. H. R. .Blank supervised a field survey in the summer of that year to determine the areas producing salt water. A.report 'titled "Sources of Salt'Water Entering the Upper Brazos IRiverm, Project 99, Texas A and M Research Foundation, resulted. All the tributaries in the upper reaches of the Brazos are intermittent except one or two which flow from sources of artesian salt water. Practically all the stream chan- nels were dry in the summer of 1954. Samples of water for Project 99 were obtained from bodies of standing water and from shallow subsurface water, assumed to be underflow, in sand bars and channel fills of stream beds. Dr. Blank concluded that the Dove Creek Salt Flat in northwestern Stonewall County contributed about 40 per cent of the Brazos River salt and that two salt flats in north- eastern Kent County were large contributors of salt. The Ambursen Engineering Corporation, Houston, Texas, did core drilling in the Dove Creek Salt Flat in 1955 and prOposed a dam for a salt evaporating reservoir. The U. 3. Geological Survey, Surface Water Branch, constructed weirs and a gaging station in the Dove Creek area of Stonewall and King Counties in 1956.. Samples for chemical analysis are taken and water flow is measured at two-week intervals. A continuous flow record is obtained from the gaging station. The results are not yet (April, 1957) calculated and released by the U. S. Geological Survey. Scope of this Investigation Upon the basis of conclusions of Project 99, A and M Research Foundation, the Texas Board of‘Hater Engineers proposed a geology and ground-water study of the four-county area to determine the source and movement of the salt water. 10 It“ saga-surfafii-L 1 The area covers about 345 square miles of Dickens, Kent, King and Stonewall Counties, Texas, and is approximately 100 miles northwest of Abilene (figure 5, p. 12.). Acknowledgments Grateful acknowledgment is due numerous individuals for valuable assistance rendered. Dr. D. C. Van Siclen and Mr. G. C. Frazer, III supplied useful geologic informa- tion. Messrs. Jack Brown, R. T. Peyton and Otis Richards, geologists of Continental Oil Company, provided much help- ful data and many sound ideas. The area ranchers, especially Messrs. G. W. Springer, W. A. Springer, Sr., W. A. Springer, Jr. and E. M. Jones, cooperated and assisted the writer in field activities on their ranches. The writer is indebted to his wife, Barbara E. McMillion, for her help and en- couragement. Much appreciation is due Mr. R. T. Littleton, Chief of Ground Water Branch, Texas Board of Water Engineers, for his patient and careful supervision. The writer deeply thanks his major professor, Dr. C. R. Humphrys, for guidance and proofing of this report. 11 Figure 5. Index map showing location of detailed area in Texas. 12 3H! GENERAL DESCRIPTION OF‘DETAILED AREA The detailed area lies in the Osage Plains section of the Central Lowlands province. Topography varies from featureless through gently rolling and scarped plains to intricately dissected terrain. Altitudes range from 1665 feet along the Salt Fork of the Brazos River at the east- ern edge of the area, to 2180 feet on the level plains at its northwestern corner. The surface has an average eastward slope of about 20 feet per mile. Local relief is comparatively large with about 530 feet as a maximum. Bedrock exposures are plentiful where local relief is ap- preciable but rare on the featureless plains. Geomorphic features of the area are results of depo- sition and erosion of sediments, with little or no effects from diastrophic movements. These features are prominent scarps trending in a north-south direction; hills and val- leys; isolated buttes; meandering river channels to deep, .almost vertically—walled canyons; and spectacular flats covered with white salt and gypsum deposits. The activities of this report are centered around three salt flats of this area. The Dove Creek Flat is in.Stonewall County near the King County line and four miles east of the Kent County line. The Short Croton Flat and Hot Springs Flat are in Kent County about two and one- Ihalf'miles west of the Stonewall County line and six and one—half miles and four miles, respectively, south of the IDickens County line. These two flats are about nine miles 15 JHE west-southwest of Dove Creek Flat. The flats are in large ranches, and access to them is difficult since these parts of the ranches are seldom used by the ranchers. l4 :IHE CLIMATE AND SOILS The climate of the detailed area is classified as semi-arid. The average annual precipitation is about 21 inches (figure 1). The annual rainfall varies from year to year, and in some years there are extended periods of dry weather. The lightest precipitation is usually dur- ing the winter. Local thunderstorms or "cloudbursts" are the usual form of rain during warm weather. Winters are mild except for several short and severe cold spells due to north winds, known as "northers". Sum- mers are long and comparatively hot. Evaporation rates are high because a very large percent of the days year- round are clear, humidity is low, and wind velocities are usually high. The soils in this area are mainly residual soils with characteristics very similar to the underlying parent ma- terial. The Childress gypsum outcrop (figure 6, p. 18) is the dividing line between clayey soils to the east and fine sandy soils to the west. Irregular-shaped bodies of wind- blown sand, called "shinnery sand", occur scattered over the area. The fine sandy soils extending west of the Childress gypsum outcrop are of principal concern in this report. They are described by the Soil Conservation Service as deep, medium-textured soils with moderate to high permeabi- lity. The texture range is from fine sand to silt loam. .At least 75 per cent of these soils are loamy sand and silt. 15 :rHE The soils are dominantly red in color due to the red color of the parent material, Whitehorse sand of Permian age. They are generally high in mineral content necessary for plant growth. These soils are easily eroded by both sheet and gully erosion. Conservation practices are the rule on land under cultivation. Less than one-tenth of the detailed area is under culti- vation. Principal crops grown are cotton, winter wheat, oats and maize. The other nine-tenths of the land is rough and often deeply dissected by erosion. This rough land is sparsely covered by such plants as mesquite, juniper, cacti and short grasses, and is used to pasture cattle. Farming and ranching are the principal sources of income for the area. 16 :rHE ring”. -. . LL STRATIGRAPHY Permian Deposition Figure 6 on page 18 shows the outcrop of the groups of series, Permian age, in the problem or detailed area and surrounding region. Triassic and Cretaceous also crop out in the region. None of the Triassic and Cretaceous rocks extends into the detailed area and thus they will not be considered further. The Permian rocks of this re- gion were deposited in the province of the Permian sea re- ferred to as the Eastern Shelf area. It is also called the Eastern Platform of the Midland basin. The Permian sea covered a large part of Texas. It reached northeastward into Oklahoma and Kansas and north- westward into New Mexico and Arizona. At many places in Texas, Oklahoma and Kansas, no pronounced break occurs be- tween Pennsylvanian and Permian sediments; thus indicating that the Permian sea was an inheritance from Pennsylvanian time (Sellards, 1932). 6000 to 6500 feet of Permian sediments underlie the surface of the detailed area. In Wolfcamp, earliest Per- mian, extensive limestone‘deposits were formed. In Leonard, the limestone was gradually replaced by dolomite, which was displaced westward by evaporites and red shale from the east. Red shale, red and some gray sandstone, evaporites, and co- casional dolomite beds continued to accumulate more or less continuously during Guadalupe._ Deposition of red-beds and evaporites continued intermittently in Ochoa. l7 :rH i A 4 ‘ ' Q V n A l ’ n e 'N .e "" «O ‘ ... ~‘.-| .... i". .o ., 54' VP“; ... . ~' _I 3 :.~ \ -.(‘v e ‘ 5 - ," ‘u 1 . ' I ~ ‘0 '1' I o -' 0 v ’. EXPLANATION (Scale: 1 inch 3 Cretaceous Cret. Uhdivided Triassic EEEE Dookum Group Permian Ochoa Series C223 Ochoa Series Undivided Guadalupe Series I: lhitehorse Group El Reno Group Leonard Series - Clear Fork Group - Wichita Group sediments. Figure 6. OutcrOp map of rocks 15 miles) Ca Claytonville Dol. 8'—-*' I9 Childress Gyp. I '50 con Guthrie Dol. 350'—$zs‘ J scam-.335, 5a. San Angelo 3s. 1 { °“‘ Morkel D01. Sod-uso' , LNG» Standpipe Ls. 225’ ‘ CM- Lueders Ls. Probable eastern extent of salt beds in Permian from Permian through Cre- taceous in problem area and surrounding region. 18 :[H The beds with surface exposures in the detailed area have a regional due west dip of 25 feet per mile which is locally modified by gentle anticlines with flank dips not exceeding 60 feet per mile. (Plates 4 and 5, pocket). Lithologic changes are more common basinward rather than along the strike. Surface erosion since uplift has de- veloped a topographic slope to the southeast which exposes the Permian beds, oldest to youngest, from east to west. Correlation Correlation of the rocks at the surface in the detailed area to those described in standard reference areas and in subsurface is very important. ~For example, salt beds seldom, if ever, are exposed at the surface because they dissolve very easily in circulating water. If salt beds are present in the subsurface of a formation, their presence may be de- tected or suspected by a knowledge of the formation as de- scribed elsewhere. L. T. Patton classified these rocks in 1950 in his brief report, The Geology of Stonewall County, Texas, The University of Texas Bulletin No. 5027. In 1932,‘E. H. Sellards,‘W. S. Adkins, and F3 B. Plummer relied heavily upon Patton's publication for stratigraphy of this area in their publication, The Geology of Texas, Vol. 1 Stratigraphy, The University of Texas Bulletin No. 5232. Since then, no publication describing the stratigraphy of these rocks has been widely distributed. The stratigraphic system of Patton .and Sellards is still prevalent in many geologic circles, 19 IHE “sixfimu despite the fact that for this area it is incomplete and out-dated. However, much detailed and accurate work has been done since 1932 by persons interested in oil explora- tion and many of these studies have been printed in the "Bulletin of the American Association of Petroleum Geolo- gists" and the "Bulletin of the Geological Society of America". Correlations used in this report are based on the Abilene Geological Society cross-section, "Scurry County to Parker County", prepared by committees of the Study Group on Stratigraphy in 1949 and modified slightly by D. C. Van Siclen in 1951 (figure 8, p. 22). This cross- section represents the best opinion of the most interested geologists active in the region. Series and systemic di- visions are those defined by M. G. Cheney in 1940, with subsequent slight modifications (1945, 1947). Permian System The Correlation Chart (figure 7) on page 21 shows the systemic classification of the Permian rocks in this area. The lowest Permian rocks at the surface in the detailed area belong to the upper El Reno group (Dog Creek forma- tion). The other Permian outcrops are all in the White— .horse group. Thus, this section on Permian rocks will discuss basal El Reno through the Ochoa series. The Ochoa is included since it is stratigraphically above the rocks cropping out in the detailed area and may influence the area hydrologically. 20 3 WEST EAST < . ' g resume OR muss": 0 Dawn LAKE o DEWEY LAN: rrrr I: HUSTLER m1.srlx..lt:'la'1 ) U SALADO 5ALADO~~ C) CASTuE BASIN REEF SHELF TANSILLFACIES u “m SILL CLAYTONVILLE 00L. LIJ FACJES «1 0- YATES g YATES 3 LL CA r ARLS- 0" 2 BE P C SEVEN 5 SEVEN R ‘ VER 5 C N ON TAN AD 3 ‘9 A Y B RIVERS ‘3 QUEEN ESKOTA DOLOMH’E _J 3 QUEEN g GRAYBURG Lewes ESKOTA < E GRAY BURG CHILDRESS Q :0: \GOAT 0 DOG CREEK CHERRY SEEP, 5AM ANDRES NE ASPERMONT DOLOMITE < E ("5” E, “N ANDRES 5”” MCCAULLEY DOLOMITE 3 ; CANYO“ o: FLOWER P01 o la 0 Q WWW 1111!- Q V5 CUT OFF GLomETA GLORICTA MERKEL DOLOMH’E‘. -‘ ' x Q: o «S . CHOZA z < é E BLACK VICTORIO YE so 3”- »SPRABERRY 3 VALE BULLWAGON DOLOMITE a U .¢ 0 m LS. PEAK ,A j RROYO LUEDERS LIMESTONE LLJ I; (REEF) B 5g. DEAN g VALERA -—1 8 A ° in Q. ADM : _ I 2 W1- u COLEMAN JUNLTlON Ls. UE co hum “ _ h. H MOR- SEDWICK LIMESTONE __] < M .— OU Pus- "CAMP COLORADO Ls. ' BLO 3ADDLE’ CREEK L5. 3: BURSUM tooxixnmzsrowc Figure 7. Correlation Of Permian rocks of detailed area with standard reference sections. (F. B. King, 1942 and D. C. Van Siclin, 1951). .3.... .11..“ ill? .....o 2.41)“... ... ....s-..1...-____=.I.l......_ . , -. ._ . .. . $1413 iIIl-II‘IIMI... .. ...-m...- u. ._ as (Iggy/.3" .. .. .. r -.. Iftiai. .. 1.3-3.... m ”"00"! u. Mfu- one am I use? an": n: anon“ nu: '1 gyros. nut ‘ use-.- use! emu-l “some; see-en “new a ve mee- ea. ' '._ Ines! C to" 0'— ' I - __ J—‘W" -- 22 Western part of Abilene Geological Society cross section, Scurry CO. to Parker CO., Texas, 1949. Figure 8. I ..--II. .3. beeoeesee . I. I...‘ ...-O.n~.- .VI.||-III¥I59I- I.I .II* I - I HI: 0 .,I' IIIII Guadalupe Series El Reno (Pease River) group The El Reno group was defined in Oklahoma to include beds from the top of the Hennessey shale up to the base of the sandstones at the base Of the Whitehorse group (Becker 1950, pp. 57-56). In Stonewall County, Texas this includes beds from the base of the San Angelo sandstone to the base of the Childress gypsum and dolomite. The entire group crops out in a north-south belt crossing Stonewall County. The basal San Angelo, about twenty-five to one hundred feet of massive sandstone and conglomerate of chert and quartz pebbles at the outcrop, thins westward and practi- cally disappears in subsurface of the eastern part of the detailed area. Detailed sample log on exploration hole no. 189 shows only a small amount of sand at interval 920 feet to 950 feet; this interval is the position of the San An- gelo with reference to the Merkel dolomite which is at 990 to 1000 feet depth. Perhaps farther west it does disappear. The San Angelo sandstone is overlain by the Flower Pot, Blaine and Dog Creek formations. -These formation names are of Oklahoma type sections and thus far have not been applied to the Stonewall County area. However, the term "Blaine" is used in Texas (Sellards 1952, pp. 178-9) to include all three of the formations above San Angelo. This is not an appropriate use of the term since it includes more than does its type section. The formations of the El Reno group are not specifi- cally described and mapped in this report since only about 23 one hundred feet Of the upper part crop out here. In general, the Flower Pot, Blaine and Dog Creek formations consist principally of red and some green shales with a few persistent dolomite beds and some sandstone. Lenticu- lar, massive gypsum beds occur in the upper part (Dog Creek). These gypsum beds are usually less than four feet in thick- ness. Series affiliation of this group-has long been dis- puted (Lewis, 1941, pp. 75-105). Some have placed it in Leonard series with top of series at the base of the Child- ress gypsum and dolomite. Others (Skinner, 1946, pp. 1857- 74; Lloyd, 1949, pp. 19-20) place it in lower Guadalupe with top of Leonard at base of San Angelo. There is a defi- nite unconformity at the base of the San Angelo. An un- conformity at the base of the Childress is doubtful; many geologists in the Abilene area contend that the Childress ~rests conformably on the El Reno group. On this basis, the El Reno is assigned to the Guadalupe series. Guadalupe Series Whitehorse_group Lloyd and Thompson in 1929 (pp. 945-56) first recog- nized in this part of Texas strata equivalent to the'White- horse group Of Oklahoma. The term is used in this report to include the beds between the base of the Childress gyp- sum and the top of the Claytonville (formerly Sweetwater) dolomite; although, the writers cited excluded the Child- ress and may have included another 100 feet of section above the Claytonville. 24 The Whitehorse crops out in most of the detailed area. Fine red sand is predominate in sharp contrast to the shales of the underlying El Reno group. Several thick, white gypsum beds reach the outcrop; these are anhydrite in the subsurface. Also, light gray to red dolomite beds crop out, and a thick salt section present in subsurface fails to reach the outcrop because of its solubility. Five lithologic formations into which the Whitehorse has been divided in West Texas and southeastern New Mexico have been traced into the general region of the detailed area in publications by Dickey (1940, pp. 57-51) and Page and Adams (1940, pp. 52-64). All five formations appear to be present and reach the outcrop. About ten feet of outcrop Childress gypsum changes westward into thirty feet of dolomite which forms the basal part of the Grayburg formation (Dickey, 1940, p. 46; Van Siclen, 1951, p. 50). This is followed by 500 to 450 feet of elastics with much red shale and salt in the lower 150 feet, and more red sand and anhydrite above. The lower elastics perhaps be- long with the Grayburg and their top at the outcrop seems to be the tOp of the Lower Eskota gypsum. The upper clas- tics, at the outcrop extends from the top of the Lower Eskota to 140 feet above it or to 100 feet above the top of the Upper Eskota gypsum (sometimes called just "Eskota" without "Upper"), correlate with the Queen formation. Above the Queen in subsurface is 400 feet of salt and in- terbedded sand which passes upward into several hundred 25 feet of sand and anhydrite, with the upper part having been traced into the outcrop of the ClaytOnville dolomite. Perhaps, the salt section represents substantially all of the Seven Rivers (salt) formation. The Yates formation is described by Van Siclen (1951, p. 51) as overlying this salt section and represented in a Fisher County out- crOp as a sandstone with large frosted quartz grains. He also states that this sandstone is 75 feet below the Clay- tonville dolomite. The Transill formation consists of the Claytonville and associated strata. Several discon- formities occur within the Whitehorse group, and a dis- conformity at its top is indicated by the absence of the lowest Ochoa series, the Castile formation. Ochoa Series The Permian Ochoa series consists of strata from the tOp of the Guadalupe series to the base of the Triassic system. In this general area it is the section from the tOp of the Claytonville dolomite to the base of the Triassic conglomerate which outcrOps in western Kent County. The Ochoa is composed of red silt and sandstone. The outcrop section is from 100 to 200 feet thick. The writer has not attempted to divide the Ochoa into groups and formations. Qilaternarxpspgsits Wind-blown sand deposits related to development of present tOpography and thinly scattered "upland" gravels are classified as the Quaternary of the area. The wind- 'blown.sand, known locally as "shinnery sand", covers fairly 26 large areas. A rather large but thin layer of this sand is near Girard, a small town west of Short Croton and Hot Springs Flats. Other large areas are along the Salt Fork of the Brazos River. None is found along Croton and Dove Creeks. This loose sand has high infiltration rates and probably influences the salt problem by rapid recharge to the water table. I Scattered cobbles and gravel were observed on a few knolls and ridges in the detailed area. These are related to erosion (pediment) surfaces. The cobbles and gravel are cherty and quartziferous. They exert no influence on the present problem. SALT PRODUCING AREAS Dove Creek Area About nine square miles or 5,760 acres (figure 9, p. 50) in the Dove Creek area of King and Stonewall Counties contribute much of the salt of the Brazos River. This salt- producing area lies in sections 196-198, 185-185, 175-178, inclusive, Block P5 H. & T.C. R.R. Survey. The salt water rises from clay in the beds of Dove Creek and its tribu- taries, eSpecially Dove Creek Flat and Hayrick Creek. The table of average discharge and average load in tons per day of chloride and sulfate at sampling points in the Brazos River Basin during the period 1949-1951, (p.52) was prepared from records Of the U. S. Geological Survey. Croton Creek and Dove Creek are the only streams of appreciable size that empty into the Salt Fork of the Brazos River between Peacock (NO. 1) and Aspermont (Na.2) gaging stations; .Aspermont (No. 2) station is downstream from the Peacock station. No measurement was made at the Peacock station Ln.l949. In 1950 the mean daily discharge between these two stations increased 52 cubic feet per second or 24 per cent, while the average daily chloride load increased 579 tons or 158 per cent. The average daily load of 579 tons :represents about 52 per cent of the average daily chloride load of 1,105 tons in the Brazos River at the Possum Kingdom station (No. 5). In 1951 the mean daily discharge between the Peacock and Aspermont stations increased 55 cubic feet per second 28 or 107 per cent; the average daily chloride load increased 469 tons or 510 per cent. This average daily chloride load of 469 tons from these two creeks was 59 per cent of the average daily chloride load of 798 tons at the Possum King- dom Dam. The Dove Creek area flows salt water continuously from an artesian source; however, this is not the situation in the rest of the detailed area. As a result of the artesian water of the Dove Creek area, the percentage of increase in run-Off and in daily chloride load between the Peacock and Aspermont stations is much greater for dry years than for rainy years, as can be seen by comparing 1950 run-off to that of 1951. The Childress gypsum is the most prominent bed in the Dove Creek area (figure 10, p. 50). In most of the area it forms the cap for pronounced scarps, but where vegetation is well established and chemical erosion is active, the Childress gypsum, with associated strata, forms rounded and low gradient slopes. Salt water rises from clay which is stratigraphically below this gypsum bed. Fresh water is obtained in the vicinity of Dove Creek Flat from sand 'which directly overlies the Childress. The base of the Childress is mapped on figure 6 (p. 18) and will be used as a reference bed in this report. The clay that produces artesian salt water is in the upper El Reno group, Permian system. It is described in the geologic sections 1, 2 and 5 on pages 52 and 52. For 29 I MAY 0 57 I IFigure 9. (Tap) View of Dove Creek area taken from a point one mile south of Dove Creek Flat. Notice the relatively low relief. IFigure 10. (Bottom) Steep bluff on Hayrick Creek show- ing El Reno clay below the Childress gypsum. Dashed line is base of Childress. The banding in the clay is alternating red and green layers. _ _.‘—- MAV e 57 T f . . a f ‘— # Figure 11. (Top) Detail of the clay shown in figure 10. Crumbly, conchoidal fracture results in this clay when dry. Compare with photo below. Figure 12. (Bottom) Same clay, as above, exposed near mouth of Dove Creek Flat. Due to the effect of being saturated with salt water, the clay is tough, hard, and resistant, forming cascades and waterfalls. 31 m.em o.oa s.mm enemaso papa ssoa woods o n.9m a.HH m.ne snowsz soon ssoao m .nam mam maa.H osossoam mosesm a com Hoe cam. hooves; mosssm 5 ass was now soemsam summom mososm a man m.an 0.90 ssossooma_ssoa sassesos oassoo a m.oe m.nm o.mn espom asoa esopesoz season n was omo m.ao pooSsooma asoa paem m n.0a and m.Hn sooooom asoa anew H 4 Hood H.am a.nm Hon sausage osoa asom ssoao o m.mm n.0H e.ao ssomsz apps ssoao m moo -mmn.a ems.m esossoam mosssm a see Hoo.a 0mm.H hospasg‘sososm o are noo.H mom, soemeam summom mousse m mam n.me Han psossoooa snow easpesos oapsoo a can w.mo can eepom egos seepesos oapson n Non moo mos ssossoom45ssoa shew m oaa ems and sooosom ssoa sHAMIII H omoa s.mm o.o H.mo peomsz asoa ssoao m one _Nom.H .mew.a esossoam mososm s ems nmo.a oom.a hospane mousse o as» noa.a mos. soowoaa season mousse m sea n.wm . and peossooma soon gaspssos oapsoo a Hon _Hss and psossooma asom paem m mead wmmMHpm mbaaoamo .pm .oom oamz .oz mnoa :a neon ownonomam moapoum madam ommnobd haflmn use: Hmmalmwma QOHmmm Ema GZHmDQ ZHmdm mmme mONdmm Ema 2H mezHom wqumzdm ad mefimqbw Qz¢ mQHmoqmo mo Mam mmm mzoe 2H Q¢OA ma4 de MGMdmowHQ madmm>4 52 the most part the clay is laminated, jointed (figure 12, p. 51), usually friable and exhibits a conchoidal fracture (figure 11, p. 51). The conchoidal fracture is due to flocculation of the clay particles. Clay particles in fresh water possess like electrical charges but when con- tact is made with certain substances such as sodium chloride in solution, these charges are neutralized and the particles collect much as does butter in a churn. The flocculation Of the clay of this area perhaps occurred when the sediments were deposited in the Permian sea. The sea at that time was very salty, since evaporites were being deposited. Flocculation structure may or may not mean that the clay is associated with salt beds. The clay is predominantly red but much green and gray clays are present. The red color of the clay, and also of the overlying sand, is a result of oxidation of detrital magnetite and ilmenite during time of deposition. The green and gray colors probably resulted when conditions Of deposition induced reduction rather than oxidation of these minerals (Miller and Folk, 1955). It has been suggested that the salt water caused the green color; however, the above explanation seems more logical, and also salt water moves to the surface through much red clay as well as green. The clay yields salt water almost entirely by slow seepage. This water collects in small rivulets and then :meves downgrade to form larger streams of flow. The clay in Dove Creek and Dove Creek Flat produces salt water from 33 3’? its surface exposures at the contact with the farthest westward outcrop of the Childress base to about one and one-half miles east of this contact. East of the 178-185 section line only a small amount Of salt water seepage in Dove Creek occurs. Hayrick Creek is the only other pro- ducer of salt water. Here seepage is about 50 feet below the base of the Childress. The creek flows south-southeast then turns and flows about one-fourth mile due east to its mouth at Dove Creek. The farthest downstream seepage is where the stream turns to the east. Directly overlying the salt-producing clay is the Childress gypsum, a ten to thirteen foot thick gypsum bed in the outcrOp; some salt water seeps from it in Dove Creek and Dove Creek Flat. The salt water seeps up through hy- dration fractures reworked by solution processes. Overlying the Childress is four to five feet of red and green laminated clay which is followed by red, loose, fine sand. This fine sand yields good quality stock water in the Dove Creek locality. Above the sand is a four foot gypsum bed which locally forms the cap for low ridges and scarps (geologic sections 4 and 5, p. 54). Geologic section 5 was measured on a l45-foot bluff at the south side of Dove Creek near the center of land section 197. This is the steepest and highest bluff in this locality. Beds from top of Child- ress gypsum to tap of Lower Eskota gypsum are exposed here. The 105-foot interval between the four-foot gypsum‘bed de- scribed above and the base of the Lower Eskota gypsum consists 54 of fine-grained, red, unconsolidated sand with a medial six inch gray dolomite. The Lower Eskota gypsum is ten feet thick, massive, white, and contains many solution cavities. 1 Another 145 feet of Whitehorse group outcrop occurs at the head of Hayrick Creek and geologic section 6 was made there. Measurements started with the Lower Eskota gypsum and continued to the tOp of Hayrick Mountain, a small butte rather than a mountain as the name suggests. Thirteen feet- two inches of fine, red sand separates the Lower Eskota from a one foot-two inch brownish red dolomite which is followed upward by nineteen feet of fine, red sand to the base of the Upper Eskota gypsum. The Upper Eskota has physical charac-' teristics similar to the Lower Eskota except that a one foot dolomitic layer occurs at its base. Alternating strata of fine, red, loose sand and thin massive, white gypsum occur in the one hundred foot interval between the top of the Upper Eskota and the top of Hayrick Mountain. Croton Creek Area The Croton Creek area of this report is in the north- eastern part of Kent County. Salt water seeps to the sur- face from red silt and fine sand of the beds and banks of the main creek, tributary creeks, Short Croton Flat and Hot Springs Flat (figure 17, p. 48). The salt water seepage occurs over many square miles and is not restricted to definite boundaries, as is the situation in the Dove Creek area. Most of the salt water evaporates, leaving a thick 35 salt-gypsum crust. Little or no run-Off of salt water occurs except during and for a few days after periods Of precipitation. The thick, widespread salt crust is readily dissolved and carried downstream during these periods of precipitation and run-Off. All Of the streams Of this area are classified either as ephemeral or intermittent. Ephem- eral streams flow only in direct response to precipitation and intermittent streams flow for protracted periods when water is received from surface or underground sources. A stream cannot erode below the gradient necessary to permit transportation of sediment load across it. Neither can a stream erode below its base level. Croton Creek has reached the low limit for both of these regulations. Its gradient is in equilibrium with its base level, its mouth at the Salt Fbrk Of the Brazos River, and with the detritus which it must transport. Thus, stream down-cutting for it is negligible and it has developed a wide-channeled, mean- ' dering course. Parts of the area in the lower reaches of Croton Creek and northeast of it for about three miles have been lowered from a high flat plateau to lbw rolling hills and valleys; however, north and west of these parts a deep- canyoned, badlands-type of topography has developed (fig- ure 18, p. 48). 'The geologic strata cropping out in this area consist almost entirely of red, unconsolidated, practically homogene- ous, very fine sand and silt, with only a few beds of white, nmesive gypsum. Geologic sections 7 through 11 were made 36 in this area. Above 27 feet 6 inches of fine, red sand in section 7 is a three-foot gypsum bed which probably is the same as the 5-foot 6-inch gypsum at the top of Hayrick Mount- ain (section 6) in King County. Overlying the three-foot gypsum is 108 feet 6 inches of very fine, red sand, followed by a 5-foot 4-inch white, massive gypsum bed (section 8). Above this bed is another thick stratum (121 feet) of this homogeneously textured, red, very fine sand; and again it is followed by a gypsum bed, this one 1 foot 2 inches thick. 56 feet 6 inches more of this very fine sand occurs above the 1 foot 2 inch gypsum. Overlying this latter sand stratum is a prominent, twelve-foot gypsum.1ayer which is pure mas- sive gypsum throughout. It is commercially mined in this area. Overlying this thick gypsum bed upward is 55 feet of red silt with a few round cherty cobbles on its surface. From the bed of Short Croton Flat to the top of the high plateau south of the flat, the combined geologic section totals 546 feet - 526% feet of very fine red sand and 19% feet of gypsum. The fine, silty sand of this area often stands as verti- cal or nearly vertical walls as high as 200 feet. In places where a cap of gypsum occurs, the underlying silt produces angles as large as 120 degrees or 50 degrees overhanging from vertical. These features are picturesque, but make access to and travel in the area most difficult and dangerous. Geomorphplogy The salt flats and other physical features of this area 57 developed as a result of erosional agencies acting upon the rocks present and the original land forms. Such a discussion is classed under geomorphology. In a narrow view, the val- leys and hills appear to be just like those seen everywhere else. However, careful examination will reveal definite con- ditions which caused their individual characteristics. In a regional sense, the present land surface consists of a series Of gently sloping plains intersecting each other or separated by faint to cliffed scarps. In the detailed area they are often dissected into hilly terrain and bad- lands by ephemeral and intermittent streams. Plains and scarps are broad features and more readily Observed and understood than valley sides and hilltOps. Plain is here defined as a circumscribed area of even surface and gentle slope. The plains are underlain by non- resistant rocks covered by little or no alluvium except lo- cally by scattered gravel. They are distinguished from dip slopes by not being develOped in a single resistant bed, al- though some do dip westward with the dip of the bedrock. Plains have developed at various levels and Often one occurs above another separated by steeper slopes or scarps, like a series of broad stair treads separated by gentle risers. The scarps range to several hundred feet high and may be continuous for tens of miles. The larger and more promi- nent are protected at the top by an erosion-resistant bed but this is not necessarily true of the smaller local scarps. {There are no thick accumulations of talus. The scarps are 38 cut back by local gullies which first attack their base and then gradually work their way to the top of the scarp. These gullies possess a characteristic steep-walled, box canyon head. The scarps are not forced back by lateral planation of streams. Most scarps have a fairly sharp change of slope at the top and the steeper scarps undergoing active erosion ordinarily have one at the base which separates the scarp from the slope at its foot. In some cases the plain below the front of a less active scarp rises continu- ously with gradually increasing inclination until at the top the slope abruptly decreases. The erosion cycle of more active scarps resembles that for desert conditions - the source of detritus lying on the lower plain is the scarp which rises abruptly above it. "Sheetwash" is the leading erosional agent and the scarps are not covered with vegetation, thus they are exposed to rapid erosion during each rain. Most of the precipitation falls as high-intensity rain and hail storms of short duration. The retreating scarps leave local areas of terrain dis- sected by deep gullies and canyons. Vegetation becomes es- tablished on these areas and simultaneously they are worn down to form rounded hills and valleys, which now are part of the plain at the foot of the scarp. Origin of Dove Creek Flat Dove Creek Plat covers about 400 acres in sections 185, 184, 197 and 198, Block F, H. & T.C. R.R. Survey, Stonewall (Jounty. Its main body is circular with elongated-upstream 59 extensions at places where streams enter. Dove Creek flows in a semi-circular course to the north around it. The drainage area of the creeks entering the flat is circular, with the center of the circle coinciding closely with the center of the flat. Its floor or bed is practically flat and slopes gently downstream to the east. The lower one-half to one-third of the floor is an exposure of red and green clay which is saturated with salt water. The upstream part of the floor is the surface of the outcropping Childress gypsum. Both the clay and the Childress gypsum are in places covered by silt deposits and salt crust. The flat is surrounded by a 50-foot high bluff. The strata of the bluff are a basal five-foot clay layer, a medial fine-grained, loose, red sand, and a four-foot gypsum bed. Clay saturated with salt water is sticky, tough, and resistant to both physical and chemical erosion. Figure 12 on page 51 shows the characteristics of the clay which forms the lower part of this salt flat. The water from Dove Creek Flat flows into Dove Creek; between the flat and this lower level the salt-saturated clay has developed cascades and small waterfalls instead of wearing down smoothly (figure 12, p.51). Cascades and waterfalls are usually characteristic of hard resistant rocks. These features have developed along a right-angle joint system in the clay. The drainage area, except areas of flowing-artesian salt water, has run-off only at periods of precipitation. Rainwash is the principal agent of erosion because of the 40 common violence of the storms, the deficiency or absence of vegetation, and the loose, sandy nature of the local regolith. Thus, the rapid run-off carries heavy loads of silt and sand. The Childress gypsum has developed a hard smooth surface where exposed as the floor of the flat, mak- ing it rather resistant to the abrasive action of sand- loaded run-off. The bluff surrounding the flat is also the scarp Of a small local plain. The twenty feet of loose sand, its main stratum, is not resistant to rainwash. With each rain much of the sand is washed away. The bluff, being capped by the more resistant four-foot gypsum bed, maintains a high angle of inclination. Since the drainage area is circular and small, the scarp moves radially away from the center of the flat. Also, the wind is usually of high velocity and proba- bly removes much of the loose sand without eroding the floor Of the flat appreciably. The Childress gypsum is more easily eroded than the un- derlying clay (figure 14, p. 42); therefore, more and more of the clay which yields salt water by seepage is being ex- posed and the amount of salt water seepage should increase as a result. . From the above study, conditions necessary for develop- ment of these salt flats are established as follows: 1. A.confluence of several streams at a place with a local base level which restricts down- ward erosion. 41 MAY 0 57 J Figure 15. (Top) Low bluffs or scarp around upper part of Dove Creek Flat. The fine sand below the gypsum bed near the top erodes readily by rainwash and un- covers the more resistant Childress as the floor of the flat. Figure 14. (Bottom) Detail of Childress gypsum shown in above picture. Solution is enlarging fractures caused by hydration; nevertheless this bed is still more re- sistant than the bluffs. 42 2. A rather high bluff or scarp composed Of sedi- ments which erode easily by rainwash and which maintain a high angle of inclination due to properties of the sediments or to a cap formed by a more resistant bed. 5. An arid type climate typified by violent storms and land sparsely covered by vegetation. Origin pf_§alt Flats of Hayrick Creek Three small areas, present on the west side of Hayrick Creek in King County, were described by Blank (pp. 9 and 10, 1955) as the Lower, Middle and Upper Salt Flats of Hayrick Creek. He attributes their origin, as well as the origin of all the other salt flatsin the detailed area, to "sap- ping" by salt water seepage. Only a small amount of salt water is produced in these areas, since most of the salt water-yielding clay is covered by thick alluvial-fan deposits of silt and gypsum talus. At the heads of these flats where the "sapping" is supposed to occur, little or no salt water seepage is present. The conditions for develOpment of salt flats, as es- tablished in the above section, can well be applied here. For the first condition, several small, ephemeral streams join at each flat and the local base level is established by proximity to the major stream, Hayrick Creek. A tribu- tary stream does not degrade below the level of the larger stream into which it flows. For the second condition, about 50-57 feet of crumbly, nodular clay, capped by the Childress 43 gypsum, forms a high angle slope. The clay, being dry and crumbly (figure 11, p. 51), is readily carried away by the driving force Of rain. Of course the climate remains fairly constant over the whole area, satisfying the third condition. Actually, these three local flats are much like valley fans. The upper parts of these areas are covered with large gyp- sum talus (figure 15, p. 45) and the fragment size of the deposits decreases downstream. These flats have a higher lepe of floor than is found in the other flats of the de- tailed area. The drainage courses Of the surface run-off have develOped around certain places in these flats, leav- ing many small isolated knolls (figure 16, p. 45). The Opposite or east side of Hayrick Creek has no promi- nent bluffs or scarps for creation of flats. The surface slopes gradually to the creek bed and vegetation is well established. Gypsum beds, elsewhere prominent in the area, form part of the surface slope. Since the surface is broad and gently sloping, this area is supplied with much sub- surface moisture for plant growth and solution Of the gyp- sum beds. Origin or Short CFBEOn.EPg-fiP§.§Q?§98§.£2232. Short Croton and Hot Springs Flats are flat, salt- covered areas spectacularly surrounded by high red silt bluffs about 110 feet high. Several small dry washes enter each of the flats. Both are tributaries of Croton Creek. The lowest gradient possible has been develOped between these flats and Croton Creek, thus the base level Of the first 44 _. _.- ._ _.___.A_.. MAY 0 57 |_ Figure 15. (Top) Talus of small dry wash entering the Lower Salt Flat of Hayrick Creek. Such talus is typical of valley fans. Figure 16. (Bottom) One of several knolls in Lower Salt Flat of Hayrick Creek. The knoll was isolated by sur- face run-off’developing its drainage course around it. These flats were formed by rainwash. 45 condition is present. There is a llO-foot section of easily eroded fine sand and silt from the base of each flat to the first gypsum bed, answering the qualifications for the second condition. The origin of these flats is essentially the same as that for flats on Hayrick Creek except that here the silt and very finesand can maintain a high angle of inclination without a cap rock at the top. In the Short Croton Flat, there is a salt water "spring" which yields about 25 gallons per minute. It is located 58 feet from the base of the nearest bluff. Realizing that elsewhere in this Croton Creek area salt water rises only as slow seepage, the writer made a thorough investigation of it. The highly mineralized water has created a very tough, gypsiferous, silty clay layer over about 200 square feet of the southwest corner of the flat. The layer averages about six inches thick and in a cavity below it is eight inches of standing water. Below this water is several feet of soft, water-filled silt. The salt water seeps up through the silt, collects under the six-inch layer, and then finds its way out by the opening called the "spring". The pic- _ ture (figure 21, p. 50) shows a hole in this six-inch layer. The hole was originally made by a cow which stepped through it and broke a leg. The above situation is odd, but il- lustrates that strong, tough deposits are formed by salty, gypsiferous water. Also evident in the Short Croton Flat is a swirling action of the run-Off water over its floor during and after 46 a hard rain. This has formed several cone-shaped holes, two to four feet in diameter, which occur between main drainage courses on the flat. This action aids in dis- tributing the sediments evenly and, thus, keeps an almost level surface (figure 24, p. 51). Salt plays its part in the formation of these flats by preventing the growth of vegetation. Thus, the sedi- ments are always bare and ready to be shifted or washed away by the force of running water. 47 _ , —--—.«--~W-.--._M—‘— -..-3 ‘l‘—‘ Figure 17. (Top) View of Croton Creek area taken from a point about 5/4 mile southwest of Short Croton Flat (white area in background). Note the high relief and barren canyons. Compare with figure 9. Figure 18. (Bottom) Closer view of canyon at left side of upper picture. The gypsum bed at the top of canyon wall is about 500 feet higher than floor of Short Croton Flat. 48 :ukm. Figure 19. (Top) llO-foot bluff on southwest side of Short Croton Flat. The bluff consists entirely of red silt and very fine sand except for a thin wavy layer of sec- ondary gypsum. The white area near the base is salt crust formed by seeping ground water. ZFigure 20. (Bottom) Detail of salt crust in upper picture. The salt has been scraped off a vertical strip just left of the shovel. 49 Figure 21. (Top) Hard, resistant, 6 to 8-inch clayey layer formed by ground water in the floor of the southwest corner of Short Croton Flat. Salt water from seepage collects under the layer and was about 8 inches deep when visited by the writer. Figure 22. (Bottom) Salt water ”spring" about 12 feet from above hole. The water which collects under the layer comes to surface here. Figure 25. (TOp) Rough, salt-gypsum crust as is typical in Short Croton and Hot Springs Flats. The salt of this crust will be flushed downstream by run-off from preci- pitatlon a Figure 24. (Bottom) Small (2 to 4 feet in diameter) cone- shaped pits occur between main drainage courses in Short Croton Flat. These were formed by the swirling action of run-off during a heavy rain. 51 Geolog}c_3ections in the Salt ProducingAreas Section 1. North side of Dove Creek at gaging station in NE corner, section 177, Block F, H. & T.C. R.R. Survey, Stonewall County. Feet Inches Childress gypsum, massive, white, fractured 9 O and weathered Clay, nodular, green 0 9 Clay, nodular and conchoidal fracture due to 26 6 flocculation, red Gypsum, Gray, platy O 2 Clay, nodular, red, silty 2 0 Gypsum, greenish-gray 0 1 Clay, nodular and conchoidal fracture, red 8 O Gypsum, white, crumbly 0 5 Clay, nodular, red 8 O Gypsum, green to gray, strongly laminated 5 0 Clay, exhibits flocculation structure (nodular and conchoidal fracture), red and green 4 6 Clay, exhibits flocculation structure, red, crumbly when dry J 5 6 Clay, exhibits flocculation structure (nodules about % inch to 1% inches in diameter), green to gray l 6 Clay, exhibits flocculation structure, red, shaly 5 6 Bed of Dove Creek Total of section 72 9 52 Section 2. High bluff west of Hayrick Creek where road crosses creek in SE %, SW %, section 176, Block F, H. & T.Ce ReRe Survey, King County. Feet Inches Childress gypsum, massive, white, many solu- tion cavities filled with red silt and powdered gypsum 10 0 Clay, green, nodular, dense and hard 1 0 Clay, red, scattered green reduction blotches 10 0 Clay, red, gypsiferous O 5 Clay, red, with green circular blotches about one inch in diameter 6 6 Clay, green, nodular, red streaks 0 8 Clay, red, nodular, a few horizontal layers Of green clay lO 0 Gypsum, gray, interbedded with red clay 0 6 Clay, red, nodular, friable 5 O Gypsum, white, crumbly, platy O 2 Total of section 44 ‘5 Section 5. North side where Dove Creek Flat joins Dove Creek, SW %, SE %, section 197, Block F, H. a T.C. R.R. Survey, Stonewall County. Feet Inches Childress gypsum, white, massive, fractured by hydration and weathering 9 6 Clay, green, gypsiferous, dense and hard 1 6 Clay, red, contains green reduction specks and then green layers, dense and hard 5 0 Total Of section _—15* Ofi“ 53 h"‘ Section 4. Bluff at west side of Dove Creek Salt Flat, sec- tion 197, Block F; H & TC RR Survey, Stonewall County. Feet Inches Gypsum, White, massive, a few dolomitic lenses 4 0 Sand, fine, red, loose 20 0 Clay, laminated, red and green, horizontal bedding planes 5 0 Top of Childress gypsum —_.a - ‘__ Total of section 29. 0 Section 5. 140' bluff on south side of Dove Creek, near cen- ter of section 197, Block F; H & TC RR Survey, Stonewall Co. Feet) Inches Soil, thin, sandy, gypsiferous 2 0 Lower Eskota gypsum, massive, white, some residual dolomitic layers 10 0 Sand, very fine, red, unconsolidated 42 0 Dolomite, dense, gray 0 6 Sand, very fine, red, unconsolidated 6O 6 Gypsum, anhydritic and dolomitic, white 4 O Sand,rfine, red, unconsolidated 20 0 Clay, red and green, gypsiferous, hard 5' 6 Top of Childress gypsum in creek bed ---..._ Total of Section 142 6 Section 6. In canyon at head of Hayrick Creek to tOp of Hay- rick Mountain in SE corner, section 195, Block F, H & TC RR Survey, King County. Feet Inches Gypsum, massive, white 5 w6 Sand, very fine, red, unconsolidated 22 0 Gypsum, massive, gray 0 4 54 Section 6, continued Fpet Inches Sand, very fine, red, loose 5 6 Gypsum, massive, white 5 0 Sand, fine, red, loose 8 2 Gypsum, white to gray, platy 2 0 Sand, fine, red, unconsolidated 55 0 Upper Eskota gypsum, massive, white, near base is 1'0" of red, silty dolomite 10 0 Sand, fine, silty, red 19 O Dolomite, brownish red, silty, breaks into thin sheets and flagstones when ex- posed at surface- 1 2 Sand, fine, silty, red 15 2 Lower Eskota gypsum, massive, white, many solution cavities 10 0 Total of section 152 ”lb Section 7. Measured on bluff of north side of Short Croton Creek about one mile east Of extreme western end of Short Croton Flat, section 1, Block OK, H & TC RR Survey, Kent CO. Feet Inches Sand, very fine, and silt, red, unconsolidated #15 V 6'“— Gypsum, massive, white 0 8 Sand, very fine, and silt, red, loose 5 10 Gypsum, massive, white, (probabl same bed as 5'6" gypsum of section 6 5 0 Sand, fine, loose, lower 4'0" saturated with salt water and thus more compact and harder 27 6 Bed of Short Croton Creek Total of section 50 11 55 Section 8. Measurements made on steep bluff at west end of Short Croton Flat and directly south of fence (north line of James Castleberry Survey, Kent County). Feet Inches Sand, very fine, red, loose, on surface covered with powdery, gypsum crust 22 0 Sandstone, fine-grained, highly gypsiferous, red with gray blotches O 5 Sand, fine, red, unconsolidated 5 6 Gypsum, massive and granular, white 5 4 Sand, very fine, red, unconsolidated 108 6 Base of Short Croton Flat --.. Total of Section 157 7 Section 9. Measurement made on east side of steep canyon which is tributary to Short Croton Flat from the south in James Castleberry Survey, Kent County. Feet Inches Silt, red, scattered cherty, round cobbles -55 O Gypsum, massive, white, pure 12 0 Sand, very fine to silty, red, unconsolidated 56 6 Gypsum, massive, white, forms small ledge 1 2 Sand, very fine, silty, red, loose, has high angle of inclination 121 0 Gypsum, massive, white (is same bed as 5'4" gypsum of section 8) 5 4 Total of section ‘ififir""jj"' Section 10. Bluff at north side of Hot Springs Flat, one- fourth mile upstream from its mouth at Croton Creek in cen- ter of Chas. Hardwick Survey, Kent County. Feet Inches Silt to fine sand, red, loose 70— 6 Gypsum, massive, white (same bed as 5'0" gypsum of section 7 and perhaps is same as 5'6" of section 6). 5 O 56 Section 10, continued Feet Inches Silt, red and green, gypsiferous O 6 Gypsum, nodular, white 0 4 Sand, very fine, silty, red, forms high angle of inclination 22 6 Gypsum, platy, gray, wavy O 5 Silt, red, salt crust on lower three feet 11 6 Silt, deposited by creek of Hot Springs Flat, saturated with salt water 5 6 Greek bed --- Total of section 62 5 Section 11. A stee bluff at the southwest end of Hot Springs Flat in SE , NE %, section 1, Block H,IH & TC RR Survey, Kent County. Feet Inches Gypsum, massive, white, (same as 5'4" gypsum of sections 8 and 9) 5 4 Sand, very fine, silty, red with grayish- green reduction spots ~ 107 0 Floor of Hot Springs Flat and top of 5'0" gypsum bed Total of section 110 '74'*‘ 57 HYDROLOGY Topographygand the‘Water Table .A tOpographic map is essential for a study of this nature; however, no topographic coverage is available for any part of this area. The only established elevations are a line of U. S. Coast and Geodetic bench marks along the Wichita Valley Railroad between Jayton and Girard in Kent County. ' Plate 2 is a generalized topographic map drawn on a contour interval of 100 feet. Elevations of 219 explora- tion holes, Oil wells, and water wells, as well as a per- sonal knowledge of the general surface features from field work and from use of aerial photographs, were used to draw the map. It shows most of the main topographic features needed for this study; however, many of the smaller features are lost because of the limited number of control points and the lOO-foot contour interval. The map showing contours on the water table_(p1ate 5 in pocket) was prepared from water levels of elevation- controlled water wells. A 50-foot contour interval is used to show as much detail as possible while sufficient control is available. Table 1 is a record of these wells. All of the water wells in the Dove Creek vicinity were scheduled and measured, unless Obstructions prevented measurement. All the wells that could be measured in northeast Kent County, south and west of the salt flats there, were scheduled and measured; however, some of the wells in this vicinity were 58 scheduled even though measurement of them.was not possible. No attempt was made to schedule water wells in Stonewall County south and east of the wells shown on Plate 5. Eleva- tions of the wells were taken by barometric method. One altimeter was kept stationary near a known elevation and readings on 15-minute intervals were made by the writer's wife. Another altimeter was taken to each.we11 and the altimeter reading and time of reading were noted. Later, the readings for the wells were corrected for changes in barometric pressure which occurred between the time of de- parture from the known elevation and the time of the read- ing at the well. The Coast and Geodetic bench marks were used as control points in eastern Kent County. In King and Stonewall Counties, the ground elevations of exploration holes and deep oil well tests were used for elevation con- trol. These elevations were determined by Oil companies in the years 1949-1952. The water table or the uppermost surface of the un- confined ground water generally conforms to the surface topography. The water table elevations decrease sharply near high bluffs and scarps and deep canyons. Likewise, it increases rapidly from these features to highly elevated, broad plains. Two localities in this detailed area illus- trate these statements. One is at the head of Hayrick Creek in King County and the other is in northeast Kent County. Hayrick Creek Canyon cuts abruptly into a broad rolling plain. The plain near the head of Hayrick Creek 59 has a few prominent buttes but then gradually increases from about 1980 feet to almost 2100 feet in a northwest direction. Southeast of the plain, elevations drop rap- idly to about 1720 feet in Hayrick Creek Canyon. The water table reflects these rapid surface changes, as can be seen on Plate 5; a drOp from 1900 feet to less than 1750 feet occurs in only a few miles. The water-table gradient at this place is about 100 feet per mile. The water table meets the surface at several places in the canyon, producing fresh.water seeps and springs. The other area having these similar topographic and water table conditions lies in northeast Kent County; there a large, rather flat plain is sharply reduced in elevation by tributary canyons of Croton Creek. Salt water seeps and springs are produced at the contact of the water table with the surface. This discussion is continued under the follow- ing section, "Source of salt water in Croton Creek area". Source of Salt Water in Croton Creek Area_ The broad plain mentioned above covers most of the west- ern part of the detailed area and extends twenty miles far- ther west where it is intercepted by the scarp of the High Plains. In the detailed area it is flat to rolling, except where deep gullies and canyons have cut into its edges. It lepes gradually from 2176-foot elevation in the north- west part of this area to 2008 feet at Jayton in the south- east part. Soils of this plain have moderate to high in- filtration rates. The water table is commonly 25 to 45 feet 60 below the surface, but much deeper depths occur near deep canyons and high scarps. The northeast part of this plain is deeply incised by canyons tributary to Short Croton Flat, Hot Springs Flat and Croton Creek itself. These canyons have vertical boxed-heads, many as deep as 100 feet. The predominent fine sand and silt have a low co- efficient of transmissibility, and thus the water table follows closely the steep gradient of these deeply eroded surfaces. The water table makes contact with the surface in the lower parts of the canyons, and in the salt flats and creek beds. Salt seepage results at this contact. Figure 25 on page 65 is a vertical section that typi- cally illustrates the ground-water hydrology of this area. This section is along a line which extends from the south- west corner of Short Croton Flat to a point about three miles southwest of this corner. The surface configuration was plotted from elevations of wells and from data of hand- leveled, geologic sections. Measurements of water wells were used to draw the position of the water table. The distance of the well locations on this illustration are not actual; the distance Of individual wells from prominent canyons or scarps was calculated and this distance was used in preparing the vertical section. An "ocean of salt water" was reported at depth 255 feet (elevation 1797 feet) in well 74 by its driller. No other reports of depths to salt water were obtained since water wells are not usually drilled much deeper than the water table and records are not gener- 61 ally kept by local drillers. The elevation of Short Croton Flat is approximately correct. Horizontal distances were measured from aerial photographs. The surface gradient from the flat to the top of the plain, as shown in the vertical section, is about 150 feet per mile; whereas, the corresponding hydraulic gradient of the water table is about 151 feet per mile. The hydraulic system is judged "unconfined" since no impermeable or thick soluble beds are present to form an artesian system, and since the salt water seepage is widespread and not re- stricted except by elevation and proximity to places of high local relief. A 285-500-foot thickness of this un- confined, saturated sand is present between the highest water-table elevation and the elevation of salt water seeps. The water moves from points of high to points of low po- tential -- in other words, from points at which the water table is high to points at which it is low. Water at point "C" of figure 25 is of higher potential than that at "B" due to difference of elevation; however, all along a vertical line intersecting "AF and "C" potentials higher than that at "B" exist because of pressures exerted by the overlying column of water with high static level. Thus, threads of water move from points throughout this uncon- fined body toward the place Of discharge at "B". Movement is slow and frictional losses in lateral movement are large due to resistance offered by the low permeability of the fine sand. For continuation of this movement over long 62 . .noapmnoamxo nonpadm non axon oom .poam souono anonm son“ pmownpdom mash moan: coda o weeds ma monsoon one .oonm moose gopoao one no thHOAphn noushupqsoaw on» wqalonm noauooo Hooapao> .mm enamam mmn_zlf moz 2 Id a I600 J , < u (A 4" 1400 3 I § In > 1200 8 < E . rm [L 4 ago m ((4 / 4/ (Z) eodw/ 2' _i- 9/ m . (IF-7 7 I: r" / .J I P {/4 U ! (0/ -- «V/ A“ /I/ / 27/ zoo I I I I 1 I 4 25 25 24. 22 20 la 16 I4- 12. IO 8 b 4 2 o Snuvu. MILES MEASURED IN HORIZONTAL. PLANE Figure 26. Determination of the eastern extent of salt de- posits in Permian rocks by noting the erratic changes of the otherwise regular westward dip of the Claytonville (G. C. Frazer, III mapped the Claytonville dolomite. along the Double Mountain Fork of Brazos River, Kent County. Top of Merkel was obtained from electric logs of wells near the mapped area.) 71 Artesian System of the Childress Gypsgm Either one of two situations can account for the un- usual way in which this artesian system has developed, since a recharge area does not 110 east or up the dip from a discharge area and since the water does not move to the surface from deep formations. The first of these is formation pressures in the clay underlying the Childress gypsum. Formation pressures are here defined as pressures due to overburden which tends to squeeze water from a stratum in much the same manner as water is squeezed from a sponge by force exerted upon it. The other situation is one in which the artesian pressure at the discharge area is produced by a very permeable aqui- fer transferring the 1arge head of a distal unconfined ground water body. Consultation concerning formation pressures was held with Dr. King Hubbert and Dr. DeWitt C. Van Siclen, both of whom are authorities in the field of ground water movement and reservoir characteristics. They presented information of proof that formation pressures do not develop unless the overburden is at least 5,500 to 7,000 feet thick with the variation depending upon the specific gravity and intersti- tial water of the overburden. Maximum surface elevation in- creases of this region are due west. Fifty miles in this direction from Dove Creek Flat to Crosbyton, elevations in- crease from 1,700 feet to 5,017 feet, but west of Crosbyton the surface increases slightly in elevation. The Childress 72 gypsum dips about 750 feet in this fifty miles. Thus a total of only 2,067 feet of overburden of the clay is pres- ent. This is less than one-half of the required minimum for development of formation pressures. Before the second situation can develOp, there must be a locality with.a water table much higher than 1,700 feet, with a very permeable aquifer connecting it to the Dove Creek area, and with an abundant source of salt. The plain of northeast Kent County (as discussed under ”Source of salt water in the Croton Creek area") lies about ten miles west of Dove Creek Flat and has a water table as high as 2,089 feet in elevation. This is 589 feet higher than the 1,700-foot elevation at the Flat. Thick beds of salt of the Seven Rivers formation, Whitehorse group, are present in the shallow subsurface of this locality. Salt beds are not logged when drilling is performed by a rotary method since the salt is dissolved by the large amount of water used for drilling. Rotary equipment is used almost exclu- sively by the oil industry today. Beforeabout 1955, cable tool drilling was predominant. Logs of holes drilled with this equipment show salt beds. A few such logs are avail- able for the region of the detailed area. The cable-tool holes closest to northeast Kent County are one at Spur (Udden, 1926) and another, Moutray Oil Company - Jones No. 1, in Sec. 511, Blk. 1, H. and G.N. R.R. Survey. Both of these holes are in Dickens County and about twelve miles northwest of Girard. Log of the Spur well records 152 feet 75 of salt and the log of the Moutray Oil Company well shows 167 feet of salt. Most of this salt consists of beds rang- ing from 4 to 75 feet in thickness and individual beds are separated by red silt and anhydrite (table 4, p. 151). These salt beds can be projected into the Girard area of north- east Kent County by making corrections for differences of land elevations and for bedrock dip. In the Girard area these beds would occur in the upper 28 to 728 feet of strata, forming a very large source of salt for solution by unconfined ground water. The contact between fresh water and salt water is about 250 feet below surface. So- lution by ground water has evidently removed much of the salt. Exploration hole 155, which is 1-1/5 miles west of Dove Creek Flat, flowed enormous quantities of salt water at a steady rate for about two days. It was the only ex- ploration hole of several drilled in this locality that produced flowing salt water.l/ The producing aquifer is very permeable since only very permeable aquifers, such as coarse sand and gravel and cavities in soluble beds, produce such phenomenal flows. The aquifer is also very .1/ Exploration hole 102 located 6% miles north of hole 155 flowed salt water from a zone about 150 feet above the Childress gypsum, whereas hole 155 produced water from near the base of the Childress. The artesian systems are not the same but may have similar characteristics, since both zones are near thick anhydrite beds. The flow of 102 is not considered further in this report since it does not di- rectly affect the problem at Dove Creek and since only a very small amount of information is available on the area near its 74 narrow in width in the Dove Creek area since only one hole of the several drilled struck it. Only very fine sand, silt, clay, anhydrite, thin dolomite, and possibly some salt are present in the shallow strata of this area. Exploration hole 155 produced salt water from a cavernous- type aquifer, since no coarse clastics occur in the sub- surface and since it is characteristic of only cavernous aquifers to be of narrow width in this area of the Permian sediments. (This statement does not apply outside this local area.) Anhydrite is present and salt beds or lenses of salt may be present here for development of the cavity-type aquifer. There are no indications or reports Of such salt deposits in the clay below the Childress gypsum. It is also difficult to infer that these heretofore unknown beds or lenses of salt are extensive enough to form a continu- ous aquifer for several miles. Ordinarily we would not expect to find extensive salt beds below such a thick gypsum- anhydrite bed as the Childress, since calcium sulfate crys- tallizes from solution before sodium chloride. The presence or absence of salt lenses in the clay beneath the Childress cannot be known except by intensive core drilling. The Childress gypsum is evidently the bed in which so- lution cavities have developed to produce the artesian system. The Childress extends persistently over the entire region as a bed 10 to 15 feet thick. It is underlain by thick, rather impervious clay which forms a lower confining layer. In surface exposures there is a five-foot, dense clay layer 75 above it. In the subsurface, the Childress is 100 per cent anhydrite. This anhydrite bed is the most competent bed in this shallow subsurface, and undoubtedly contains many fractures which act as avenues through which ground water can move and enlarge by solution. Anhydrite is only slightly soluble in pure water but if sodium chloride is present in the water, its solubility is much greater (Sellards and Baker, 1954, p. 625). Thus the subsurface Childress is vulnerable to the dissolving action of this area's salty ground water. It should be carefully noticed thatthe cavernous arte- sian system does not extend to the surface, but that the salt rises at the surface as slow seepage through a rather im- _permeable clay. Stand pipe measurements in the clay pro- duced only small artesian heads. Maximum was about 60 feet lower in elevation than the tOp of the 45-foot drilling rig at exploration hole 155. The explanation of this unusual situation throws muoh.1ight upon this study and much weight in favor of the Childress gypsum-anhydrite being the highly permeable aquifer of this artesian system. In order to ac- complish solution by ground water, the ground water must be able to maintain a continuous circulation through or in contact with the soluble rock. The circulation is through original permeability in the soluble rock or through per- meability of rocks in contact with it. Anhydrite is CaSO4, but when exposed in shallow subsurface and at the surface it chemically combines with water, a process known as hy- dration, and becomes gypsum, CaSO4-2H20. The hydration of 76 anhydrite to gypsum increases the volume of the bed by 55 per cent (Sellards and Baker, 1954, p. 625) and large pressures are generated. Where the bed is exposed in the outcrOp, the pressures produce in the resulting gypsum many fractures, known as hydration fractures (figure 14, p. 42). But if room for expansion is restricted by over- burden, these pressures close the fractures of the chang- ing anhydrite, thus producing a water-tight bed through which no ground-water movement is permitted. As was pointed out previously, hydration of an anhydrite bed extends into the subsurface and a transition zone exists where some gyp- sum and some anhydrite occur together with hydration being accomplished when weathering conditions are proper and ex- pansion is possible. For the Childress gypsum, the transi- tion zone seems to extend along Dove Creek for about 1% miles west of Dove Creek Flat. Figure 27 on the next page is a generalized diagram showing this artesian system. The unconfined body of ground water in the vicinity of Girard, northeast Kent County, is here shown to be the source of the water and salt. The water moves into and up the dip in the Childress anhydrite at first through original fractures, but later through cavities developed by solution, toward the place of dis- charge - the Dove Creek area. Perhaps most of the movement is in the lower part of the anhydrite bed since downward movement is restricted by the relative impermeability of the underlying clay.. When the water reaches the transition 77 SAND AND GYPSLM BEDS M—w-—PRETOMINATELY‘WNE SUREACE-rr WATER TABLE I FHiSH WATER FRESH-SALT WATER CON TAC T SALT Figure 27. Siam Sy hydrite County, the undo Creek area. _ _~_ ...—A PAGF CJREEK FIT LAT 8 RO'TON A k. SHORT CROTON FLAP sALT WATER SURFACE CFQEEK ‘\ / I / “I I AQTES'AN SALT WATER DC)VE (J‘I’ HORIZONTAL DISTANCE Generalized diagram showing the way that an arte- stem could develoo up the dip in the Childress an- . The high water table near Girard, Kent 18 conveniently shown as the source of recharge 2?? pressure but does not necess at Y in the ~gypsum. . arily have to be. Circulating ground water develops 7 i Childress but when the anhydrite-gypsum transition eone is reached the water moves out of the Childress into Flying clays and emerges at the surface in Dove cavity system _fllOO 12000 ~WSOO «IBOO -I7OO «ICOO 4500 EA LEVEL ‘ 5 IN FEET ABOVE MEAN ELEVATION zone of hydration, it can move no longer in the Childress since the fractures have been closed by expansion. Also, the contact between this bed and the underlying clay per- mits no movement of water in it because of this same ex- pansion. Thus, the water moves from the Childress and comes to the surface by the way requiring the least pressure. Perhaps the fine sand above the Childress is more permeable than the clay below the Childress, but this artesian water moves more easily through the clay since it has some per- meability and since it is about fifteen feet stratigraphi- cally below the sand. The water does not follow a smooth regular course through the clay but works its way through the often irregular fractures and more permeable parts of the clay until a point of egress is found. Its lowest move- ment is to 50 feet below the surface of the main flat or about elevation 1650 feet. 'Water under pressure of the large head of a ground water body with high-elevation water table is transmitted to the cavernous system of the Childress anhydrite-gypsum. The water confined within this cavernous anhydrite develops an artesian system. This confined water transmits pressures almost as well as an Open body of water due to the relatively large cavities in Which it is contained, however, there is a gradual loss of pressure due to resistance in movement along the walls and floor of the cavity system. At the place near Dove Creek Flat where the water moves into the low-permea- bility clay, a rapid drop of pressure occurs. 79 The chloride content of the water from boring 0-4 in Dove Creek Flat is almost three times as high as that of the water from the brine spring in Short Croton Flat and the sulfate content is almost twice as high (table on p.57). As shown in figure 27 (p. 78), the water to the Dove Creek area moves through an additional SOC-foot interval of strata with much salt and gypsum and then moves through the soluble Childress. Thus the water becomes much more mineralized than that of the Croton Creek area. The Dove Creek area is the only known place along the outcrOp of the Childress gypsum in the Central Texas region that produces artesian salt water. There is a very definite and important reason for artesian salt water coming to the surface here. A careful examination of figure 6 (p. 18) reveals that the base of the Childress crops out in the Dove Creek area about two miles farther west than at any other point along it.§/ This means that the base of the Childress is about 50 feet lower here than at any other place in the region, since the bedrock dips west 25 feet per mile. As stated before in this report, a stream does not develOp a gradient less than that required to transport its sediment load and here, Dove Creek and Salt Fork of the Brazos River have both reached this low gradient. In this area the course of Dove Creek is east-west and the course g/’ The reader should note that the Geologic Map of Texas (Sellards, 1933) shows the outcrop of the top of Childress gypsum with about five-mile east-west inaccuracies of the outcrop in this region. 80 of Salt FOrk is northeast—southwest. At a point ten miles upstream from their junction, Dove Creek has cut deeper into the north-striking strata than has Salt Fork. Hence the tributary, Dove Creek, has cut deeper into the Childress gypsum and moved its outcrOp farther west. At some time during this downcutting, a critical elevation was reached in the Dove Creek area and salt water was able to move from the Childress to the surface. The flow at first was very small, but as solution cavities developed in this bed, pressures increased and produced more discharge. 81 SUGGESTED METHODS FOR DECREASING AMOUNT OF SALT WA ER In the introduction of this report it was pointed out that different land uses, particularly conservation measures, have reduced the future run-off by about 45 per cent of the run-off before these practices were begun. Under ”Source of salt water in CrotonCreek area" it was explained that conservation practices on cultivated land, especially in northeast Kent County, increases recharge to the water table and this in turn increases the amount of ground water dis- charged which here is mainly salt water. The Brazos River Authority plans to spend $7,500,000 to reduce the amount of salt entering the Brazos River from this area. Every possible method of reducing the quantity of this salt should be carefully considered and evaluated. Reduction of~§alt in Dove Creek Area Several methods for reducing the amount of salt from the Dove Creek area have already been suggested by Ambursen Engineering Corporation and H. R. Blank. These suggested methods and other possible methods should be considered in light of this present study. These are: l. A.dam at the mouth of Dove Creek Flat. This idea has been most strongly pushed by the Brazos River Authority and Ambursen Engineering Corporation. It features a salt-water evaporation reservoir in the salt flat. The height of the water in the dam is hOped to step the is- suance of salt water by‘a stand pipe effect. However, evapo- ration is very high in the area and water removed by evapora- 82 tion will be replaced by more salty ground water during extended dry periods and crystallization from solution will produce a large body of salt. At periods of run-off its tributary streams will add large amounts of silt and fine sand to the salt being crystallized (a study of this sediment load should be made). The reservoir will in time be filled with salt and clastics and will remain as part of the integrated drainage system of the Brazos River, al- ways subject to overflow, leakage and destruction by flood. The water in the reservoir will be subject to much leakage through the thick Childress gypsum above the salt-water- saturated clay and the fine sand above the Childress. A cavern about ten feet high and five to six feet wide (fig- ure 28, p. 84) is in the bluff on the south side of the flat and upstream several yards from the proposed dam site. Local reports are that the cavern extends underground for about one mile and then comes to surface again downstream onDove Creek. Some persons say they have crawled through it. This cavern is only one of many solution cavities in the Childress gypsum which crOps out all around the lower part of the Dove Creek Flat. Nearby water wells produce good stock water from the sand which overlies the Child- ress and which forms the bluff around the upper part of the flat. Leakage to this sand would contaminate the water of these wells, therefore, if a dam is built a carefully— planned dike system around the flat should be considered. The reservoir will have to be large enough to hold not 83 Figure 28. (Top) Cavern about ten feet high in the Childress gypsum at a place several yards upstream from the pro- posed dam site on Dove Creek Flat. Figure 29. (Bottom) Salt crust forming in Dove Creek Flat. The picture was made two days after a hard rain. The crust may become several inches thick before another rain. 84 just the run-off from the largest single rain that may oc- cur, but the largest series of rains that occur during a period of low evaporation plus the amount of water already in it. A diversion system for the surface run-off could be devised. 2. The above dam.modified by grouting the ex- posures of clay It was very well reasoned that grouting the clay with an impermeable substance would step the emergence of the salt water. Uncovering of the clay,*the reverse of grouting, at this elevation is the process that has made possible the development of this artesian system. It should not be for- gotten that the solution cavities in the Childress, as pos- tulated in previous discussions, have enlarged greatly since the beginning of this development and as a result larger pressures are transmitted to the Dove Creek area since less is lost enroute by resistance. There is a possibility that this water under the increased pressures, when confined by a grouting of the clay through which it now gains relief by movement to the surface, will break out elsewhere and possibly upward into the sand above the Childress. There- fore, the writer strongly suggests that the artesian pres- sure in the Childress be measured and the possibility of the water finding other means of egress should be studied. An associated dam would have the same disadvantage as pointed out above. 3. An evaporation basin away from the immediate 85 drainage system. . A large basin could be constructed in tight clay or silty clay away from any permanent drainage courses and the salt water pumped from the Dove Creek area to it where evaporation would remove the water, leaving salt deposits. This method is used quite successfully near Carlsbad, New- Mexico, where a similar salt-water problem occurs in the Pecos River. This method has several advantages. It is away from the river system and thus chances of the salt getting back into the river are lessened. There is less possibility of contamination of fresh water sources, since it would be constructed in an impermeable stratum or strata. It could be located in a much smaller watershed of lower 10- cal relief than that of Dove Creek Flat and thus would re- ceive less sediments from run-off. Its chances of destruc- tion and overflow by floods would be little or none. The initial cost should be less than that of the dam. Several disadvantages of this method can be enumerated. Since the immediate area has no suitable locations, the salt water would have to be pumped for a considerable dis- tance eastward where many clayey soils and subsurface oc- cur. The pumping of salt water requires special equipment of high cost due to the corrosive action of salt. However, a fiber hose works better than metal ones since the salt water seeps through the fiber, evaporates, and leaves a sturdy impermeable layer of crystalline salt around the 86 hose. Maintenance and operation of this pumping equip- ment would be fairly expensive. The salt water rises ever a large surface by slow seepage and during hot, dry weather much of the seepage is immediately evaporated, forming a widesPread, thick salt crust which is flushed by flash floods common in this area. Thus, means to catch this salt for transference will be difficult and expensive to devise and operate. (Figure 29, p. 84) 4. Disposal into deep subsurface Diaposal of oil-well brines is usually by reinjection into the subsurface. Often the brines are injected into strata other than those from which they came. Such disposal of the Dove Creek salt water is possible and has the big advantage of being completely away from the surface and zones of usable ground water. The deep subsurface here is under low pressures and disposal by gravity may be possible. Anaerobic bacteria rapidly grow in water which.has sur- face exposure. When this water is injected into a permeable stratum the anaerobic bacteria cause chemical reactions, especially with sulfates, which form solid substances that plug the interstices of the stratum. This plugging is more effective in sandstones and conglomerates than in lime- stones, and limey reef structures. The Ellenburger is a loo-foot thick, extensive limestone at depth from surface of about 6,700 to 6,800 feet. The great expense of drill- ing this deep practically rules it out; however, a dry oil- test hole could be used if this deep and close enough to 87 this locality. The Coleman Junction limestone, also about 100 feet thick, lies about 5,100 to 3,200 feet below the surface. It is permeable and under low pressure, thus, it is a bed that should be studied if deep-well disposal is sought. Disadvantages are essentially the same as for suggested method 5. Expense of drilling deep holes must be added to it. The water will not have to be pumped as far as in method 5. 5. Commercial salt industry Today most commercial salt is produced inexpensively by mining from pure or almost pure rock salt. But only a few years ago the salt brine industry was a_chiefindustry in many regions, particularly in the Appalachians. The salt water (brine) was pumped from the ground and evaporated in huge vats over fires. To the writer's knowledge, no consideration has been given the idea of a subsidized salt industry in the Dove Creek area. Most persons to whom this plan was mentioned seemed to think that such an industry could not compete on a commercial scale, and therefore considered the plan worth- less. However, this salt industry would not be one of pure competition, but one of competition with considerable sub- sidization by funds allocated for the disposal of this salt water. An estimated 450 to 500 tons of chloride flow from this area daily. Thousands‘of kilowatt hours of solar 88 energy are being wasted in this sun-baked semi-arid region. $7,500,000 will be spent to lower the salt content of the water of this area. Perhaps some interested salt-producing company can develop an inexpensive system of producing this salt by the sun's energy. (A simple system of Open vats could be used.) Such a works at first should be heavily subsidized but later might become self-sufficient. The remoteness of the area is probably the biggest factor against this suggestion since transportation costs are high on cheap, bulky products such as salt. Better roads would have to be built for local access than would be needed for the other suggestions. Impurities in the water may be expensive to remove, but on the other hand, valuable substances may be present. Solving the problem of the wide- spread salt crusg described in method 5, could also be a disadvantage of this proposal. This method of disposal completely removes the salt from the area. It has an added advantage of promoting local economy. This suggested method should not be overlooked. Reduction of Salt in Croton Creek Area The conditions under which salt occurs in Croton Creek are briefly summarized as an unconfined ground-water body with a very steep water-table gradient causing movement of fresh water downward through salt beds and then laterally to emerge at the surface as highly mineralized water. It emerges as seepage in a large part of the Croton Creek drain- age system; the seepage quickly evaporates leaving crystal- 89 line salt and gypsum, and producing little run-off. The five methods suggested for reducing salt in the Dove Creek area could not be applied as effectively in this area. However, earthen dams across the mouths of Short Croton and Hot Springs Flats were suggested by Am- bursen Engineering Corporation. The sites are suitable for only low dams, less than 50 or 40 feet high. The drain- age areas of both of these flats consist of steep, barren, silty badland. Heavy storms cause immediate run-off which rushes down barren canyons.and bluffs into the flats with tremendous velocities and unusually large sediment loads. If these little dams withstand the storms, they will soon be filled by the large amount of silt carried in run- off. Thus, a new flat would be formed at this higher level. The higher level would have the effect of temporarily low- ering the gradient of the water table. A lower gradient would produce less discharge at this particular place, however, discharge approximately equals recharge and in- creased discharge would be produced elsewhere in the Croton Creek drainage system. Very little benefit can be gained by the construction and Operation of these dams. The hydraulic gradient to the discharge area can be lowered, thus reducing the rate of discharge by lowering the water table on the plain in northeast Kent County. This can be accomplished by development of intensive irri- gation from wells. Above the salt-fresh water contact there is at least 225 feet of fine sand saturated with 90 fresh water. Most of the soils of this area are under cultivation and are productive when sufficient water is available. There are six to eight irrigation wells in this area at the present time. The local farmers seem to be very much interested in development of irrigation on their farms, but they need technical aid and encouragement. The average farmer cannot afford such technical help. Research needs to be done on the development of wells which will produce large quantities of water from this fine sand and silt. This ground water contains much gypsum and the effect of this gypsum on the soils needs to be studied. Also, the possibility of salt-water intrusion into irrigation wells should be studied. This research will have to be done by state and/or federal agencies since such a program cannot be supported by the local economy. If the results of the studies are favorable, the farmers should be informed and encouraged to make use of this water. Thus, intensive irrigation would be established in the area. The water table will be lowered many feet and will possibly drop beneath the elevation of salt water discharge in Croton Creek. The salt content would be reduced in this whole area of Croton Creek rather than just in the two flats. Not only will the salt seepage be reduced or completely stopped in the creek, but also a large irriga- tion program will be developed which will improve the local economy greatly. The expense to those concerned 91 with reduction of this salt would be much less than that of any other suggested method. If the ground water of this area is connected with the Dove Creek area as illustrated in figure 27 (p. 78), the lowering of the water table here will loWer pressures and flow of salt water in the Dove Creek area. 92 SUGGESTIONS FOR FUTURE STUDIES The amount of salt carried by a stream cannot be de- termined by just analyzing samples of the flowing water - the stream discharge must also be measured and the two calculated together. This must be performed over a rather long period of time to derive an average. H. R. Blank, in one summer and part of another, made samples of low stream flows, standing water, and assumed underflow of the upper watershed of the Brazos River. Stream flows were not measured, thus the samples of these flows are practically meaningless since they do not give the quantity of salt being carried. Standing bodies of water are not representative of a stream since the salinity of such water increases rapidly as evaporation takes place. It is not likely that underflow is of the same chemical quality as the flow of a stream. First of all, the chemical quality of these streams are not consistent. During long dry periods, thick salt crusts accumulate in parts of these streams and this salt is flushed by run-off from precipi- tation. The first part of the run-off dissolves the salt and thus, run-off afterwards will be much fresher. It is more logical to assume that the channel fills and sand bars will be recharged by the last part of the run-off from a single period of rainfall. This is evident in the situa- tion of Croton Creek area. In parts of this creek a thick salt crust is formed during dry periods and no run-off occurs during these periods. A little farther downstream 93 the channel fills contain water suitable for watering stock. In prior years, ranchers in this area would scoop out basins in the bed of the creek and their cattle would drink the water which seeped into it (E. E. York, personal conversation). From the table on page 52, observe that in 1950 the Salt Fork of the Brazos River contained 420 tons of chloride daily at the Peacock Station (No. 1). This station is up- stream on the Salt Fork from Dove Creek and Croton Creek. The 420 tons is about 40 per cent of the average daily chloride load of the River at Possum Kingdom Dam (station No. 5) in that year and it is 73 per cent of the 579 tons of chloride entering the river from Dove and Croton Creeks (difference between the Salt Fork at Aspermont and at Pea- cock). In 1951, the percentage of these comparisons are only about one-half as high. The large percentage differ- ence is accounted for by a large difference in rainfall in these two years. The salt entering the Salt Fork above the Peacock station is assumed to be of unconfined ground water origin and not of an artesian source as that of the Dove Creek area; thus more salt was flushed out of this upstream area in 1950, wetter year, than in 1951, the drier year. The salt load at Peacock is apparently a large part of the salt in the Brazos River. Undoubtedly there are 10- calities upstream from the Peacock station that are large producers of salt. Some of these localities may have situations that can be alleviated by such a simple, inex- 94 pensive method as the writer's main suggestion for the Croton Creek area. This salt problem of the Brazos is large enough to justify a rather intensive program of stream gaging with chemical analyses made simultaneously, such as is now being done in the Dove Creek area. Such a program would give conclusive results and will serve as a yardstick of future chemical quality of the River. Eastern Extent of Salt-beds in Permian Depgsits Figure 50 (p. 96) shows the locations of thirteen cable-tool holes in and near the detailed area. Drillers' logs of seven of these holes show thick sections of salt, most of which is correlative with the Seven Rivers forma- tion, Whitehorse group§/. However, in a regional sense the Permian salt beds have an eastern extent which runs from northeast to southwest, as shown in figure 6 (p. 18). Salt-forming conditions are present in a sea of deposition when evaporation equals or exceeds the rate of inflowing water and the sea becomes so saline that crystalline salt is deposited. The Permian sea of the Eastern Shelf Area progressively retreated from north to south. During this retreat salt-forming conditions were present along the northern margin of the sea, so that salt beds occur in older formations northward to younger formations southward _s/ A partial record of these thirteen holes is in Table 2. Table 4 contains the drillers' logs of numbers 88, 95, and 98. These logs typically show the salt sections of this area. 95 .mea 3 eeeaeeee flee .0. .won ad wouaoooa was» on rnY. .Anda so some . vacancy send poaadaoo one uses one nu anoamdsvo HooanoHnUO he? e336 e33 eeeeude me seepage menses. as. .8 933a \l l l.‘ 96 (Sellards, 1952, pp. 185-186; King, 1942, pp. 750-751). Erosion since deposition and uplift have develOped a sur- face slope to the southeast which exposes the Permian rock oldest in the east to youngest in the west. Com- bining these two conditions of salt-bed deposition and surface erosion, salt beds are found in the shallow sub— surface in a band from northeast to southwest. The band is irregular due to irregularities in the sea of deposi- tion and in the present drainage system. To the writer's knowledge, no economic importance has been attributed to a map which would show the position of these salt beds in the shallow subsurface. However, this Ipresent study has revealed several reasons this information is valuable. Peeple living in areas adjacent to localities where salt beds are known to occur are afraid to risk drilling very deeply for ground water since they believe that all of the local subsurface contains salt. But if their locality is east of the eastern extent of the salt- forming conditions for that area, their beliefs are un- founded and useable ground water may occur there. Thus, ground water develOpment in many areas of the state could be improved by a correct knowledge of the location of these salt beds. Surface reservoirs for towns in areas near shallow salt beds could more easily and efficiently be located if knowledge of salt beds were available. Petroleum geologists are interested in the locations of salt beds which are being removed by circulating ground 97 water since slumping after solution causes pseudo- structures and the outcrops cannot be used for geologic mapping (figure 26, p. 71). 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H., and Thompson, W. C., 1929, Correlation of Permian outcrops on eastern side of the West Texas basin: Bull. Amer. Assoc. Pet. Geol., vol. 15, pp. 945-56. Lloyd, E. R., 1949, Pre-San Andres stratigraphy and oil- producing zones in southeastern New Mexico - a progress report: New Mexico Bur. Mines and Mineral Resources Bull. no. 29, pp. 19-20. Lowry, Rdbert L., 1946, An inventory of the surface water resources of Texas: Texas Bd. of'Water Engrs., Austin, Texas. Lowry, Robert L., 1955, Run-off in the Brazos and Colorado River Basins: Prepared for the Texas Electric Service Company, Austin, Texas. Meinzer, O. R., 1925, Outline of ground-water hydrology: U. S. Geol. Sur. Water-supply Paper 494. Miller, D. N. Jr., and Folk, Robert L., 1955, Occurrence of detrital magnetite and ilmenite in red sediments - New approach to significance of red beds: Bull. Am0r. Assoc. Pet. Geol., vol. 59. ‘ Page, L. R., and Adams, J. R., 1940, Stratigraphy, eastern Midland Basin, Texas: Bull. Amer. Assoc. Pet. Geol., vol. 24, pp. 52-64. Patton, L. T., 1950, the geology of Stonewall County, Texas: Univ. Texas Bull. no. 5027, p. 760 101 Pettijohn, F. J., 1949, Sedimentary rocks, 526 pp., New ‘York, Harper and Brothers. Rich, J. L., 1950, Flow markings, groovings, and intra- stratal crumplings as criteria for recognition of slope deposits, with illustrations from Silurian rocks of Wales: Bull. Amer. Assoc. Pet. Geol., vol. 54, pp. 717-40 0 Rich, J. L., 1954, Origin and evolution of rock fans and pediments: Bull. Geol. Soc. Amer., vol. 46, pp. 999- 1024. Rich, J. L., 1951, Three critical environments of deposi- tion and criteria for recognition of rocks deposited in each of them: Bull. Geol. Soc. Amer., vol. 62, pp. 1-20. Roth, Rdbert, 1957, Custer formation of Texas: Bull. Amer. Assoc. Pet. Geol., vol. 26, pp. 452-54. Roth, Rebert, 1945, Permian Pease River group of Texas: Bull. Geol. Soc. Amer., vol. 56, pp. 895-908 Roth, Robert, 1942,‘West Texas barred basin: Bull. Geol. SOC. Amara, 7010 53’ PP. 1659“].674. Sellards, E. H., and others, 1955, Geologic map of Texas. Sellards, E. H., Adkins, W. S., and Plummer, Ft B., 1952, The geology of Texas: Univ. Texas Bull. 5252. Sellards,‘E. H., and Baker, C. L., 1954, Geology of Texas, vol. II, Structural and economic geology of Texas: Univ. Texas Bull. 5401. Skinner, J. W., 1946, Correlation of Permian of“West Texas and Southeast New Mexico: Bull. Amer. Assoc. Pet. Geol., vol. 50, pp. 1857-74 Tomlinson, C. W}, et a1, 1940, Classification of Permian rocks: Bull. Amer. Assoc. Pet. Geol., v01. 24, pp. 557-58. Udden, J. A., 1926, The deep boring at Spur: Univ. Texas Bull. 565. 102 Van Siclen, D. C., 1957, Cenozoic strata on the south- western Osage plains of Texas. Van Siclen, D. 0., 1951, Ancient organic reefs of a West Texas area. West Texas Geological Society, 1949, Stratigraphic problems committee, L. S. 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Rector Survey, King County 550' from N line and Phillips Petroleum from E line, Sec. 429 C0. Blk. D, H 8: TC RR Co. Survey, Kent County Arkansas Fuel Oil 960' from W line, Sec. Co. 120, Blk. F., H & TC RR Co. Survey, Stone- wall County Center of NE %-of NE%- Sec. 105, Blk. D, H & TC RR Co. Survey, Stonewall County Peer Oil Corp. 1520' from W line and from N line, Sec. 57, Blk. 7, H & GN RR Co. Survey, Kent County Douglas Oil Co. 200' from N line and 200' from'w line, Sec. 151, Blk. G.,'W &‘NW Survey, Kent County The Texas Company 113 Year Drilled 1913 1927 1927 1926 1926 1927 1927 1926 Partial record of oil-test holes drilled with cable Ground Elevation Feet above M31 2355 2271 1706 1732 1740 2398 Table 2. Partial record of oil-test holes drilled with cable tool equipment in and near the detailed area--cont'd. Ground Elevation Year Feet above No. Location Driller Drilled Msl _~___ 95 In center of the F. P. Zoch 1927 -- SW i’, 360. 153, Elks D, H & TC RR 00. Sur- vey, Stonewall Co. *96 330' from 3 line and Atlantic 011 Prod. 1930 2256 from W line, Sec. 60, Company Blk. G., W & N RR Sur- vey, Kent County ‘*97 1980' from.N line and Marland 011 00. of 1925 -- 660' from W line, Sec. Texas 11, Blk. 4, H & GN RR Co. Survey, Kent 00. *98 In sw Corner of Elk. Marland 011 Co. a 1928 -- K, Sec. 49, T. A. Texon Oil Co. Thomson Survey, Kent County 99 550' from 8 line and General Crude Oil 1958 -- from E line, Sec. 571 Blk. 2, H&'I‘C RRCo. 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Drillers' logs of cable-tool holes numbers 88, 95, and 98 which show typical salt sections in and near the detailed area. WELL N0. 88 CASING RECORD: red rock 12%" 520' red sand 10 1290 lime 8% 2155'5" red rock lime Cellar 0-8 Salt Red sandrock 19 red rock & shells red rock 70 sdy shale red sandrock 85 red rock red bed 95 lime red sand 105 sdy shale red bed 120 red rock red bed 8c gyp strks 155 lime red rock 145 sand hard sand rock 150 no report red rock 165 sand red rock & gyp red shale strks 175 gOp lime by corre- red rock 185 lation w/ Blackwell gyp rock & gravel 205 is at 1097 salt water at 200 red rock red rock 220 grey lime lime 240 salt & gyp rock red rock 255 lime shells red quick sand 264 blue shale hd gyp rock 280 red rock red bed 517 no report lime shell 320 lime red bed 335 grey sand 1% bbl W red rock 540 red rock gyp water 545 salt gyp & gravel 560 grey lime 550-559 lime blue shale salt 455 hd grey lime red bed 465 blue shale show gas salt 475 lime 490 light grey lime salt 512 dark grey lime lime 525 blue shale salt 550 grey lime lime 540 pink shale & light red bed 575 grey ls red rock 620 hd light grey lime salt 645 hd grey lime(1t.) red bed 650 hd grey lime hd lime 665 blue shale red sand 675 bkn lime shells 151 680 685 715 750 740 750 785 860 895 925 955 970 980 985 992 1002 1065 1097 1114 1150 1150 1165 1180 1195 1200 1205 1211 1215 1228 1255 1270 1255-70 1288 1521 1528 1556 1545 1568 1515 1700 1708 1722 Table 4. Drillers' logs of cable-tool holes - continued. 'WELL NO. 88 Cont'd. less than % bbl. water 1740-50 grey lime sdy 5 bbls. per hr. Rainbow at 1728-52 hd dk grey lime light grey lime red rock grey lime red beds hd grey lime blue shale red rock lime gray lime brken lime brown shale by sample 3 est .by Wichita Albany 2605 brkn lime blue shale brkn lime grey lime blue shale lime shells grey lime brkn lime grey lime black lime CASING RECORD: 20 19'4" 151 342 12 1050 10 1542 8% 2625 red rock brkn lime gravel HEN red rock salt red sand red rock & salt grey lime 5515 brkn lime 5546 1758 black lime 5569 brkn lime 5591 lime 5450 1790 , brkn lime 5515 1896 SLM 5528 1962 brkn lime 5575 1985 dk grey lime 5595 2055 bkn lime & shale 5610 2110 dk grey lime 5620 2116 blk slate grey lime 2141 shells 5655 2145 grey lime 5645 2445 slate & lime shells 5660 2480 light grey lime 5705 grey lime 5760 dk grey lime sdy 5770 salt water % bbl. per hr. 2545 gray lime 5802 2575 dk gritty lime 5815 2620 grey lime 5850 2880 light grey lime 5865 2895 salt water 5855 4 bbl. per hr. 5065 dk grey lime 5085 grey lime 5950 5105 gritty lime almost white 5945 5165 HEN 10% sand 5184 TOTAL DEPTH: 5945' WELL NO. 95 white lime 550 anhy & red rock 550 red sand 560 red rock & salt 600 red rock 650 hd lime 700 salt 725 0-500 Iime 755 520 soft salt 775 550 red rock 800 562 red rock & salt 860 447 brkn lime 875 457 red rock 900 540 salt 920 anhydrite 940 152 5865-5870 Table 4. Drillers' logs of cable-tool holes - continued. WELL NO. 95 Cont'd. salt 965 anhydrite 2480 anhydrite 970 shale & red rock 2490 red rock cave 985 blue shale 2575 salt 995 lime hd 2590 red rock 1055 anhydrite 2595 red sand 1050 lime 2605 salt 1070 red rock anhy 2620 red sand 1080 lime soft hd 2640 red rock salt 1475 anhy & red rock 2680 lime shells lime hd 2695 sdy hard 1490 blue shale & anhy 2700 red rock 1505 lime hd dark 2750 anhydrite 1515 shale soft 2745 white sand HEN 1552 lime brkn 2750 lime coarse 1558 lime black 2755 lime fine 1545 blue shle & anhy 2785 slate 1575 lime grey 5060 lime white hd 1610 lime brkn 5065 lime & slate 1670 lime hd 5075 lime & slate 1670 blue shale 5085 salt 1675 anhy & shale 5110 llme 1700 lime brkn 5120 shale 1705 lime black 5495 lime 1715 dark shale 5500 lime brkn slate 1855 lime 5925 lime hd 2055 lime brkn 5955 anhydrite 2070 lime black 4150 lime hd 2090 lime brkn 4145 brkn lime soft 2100 lime 4150 lime hd 2180 anhy & shale 4165 lime dark 2195 lime 4190 sand white 2200 lime brkn & shale 4205 lime 2515 lime 4475 sand HEN 2555 sand HFW 4508 lime brkn dk 2595 sdy lime grey 2598 lime dark 2470 TOTAL DEPTH 4508' WELL N0. 98 CASING RECORD: surface red sdy 0-110 20" 275' anhydrite, White 125 15%" 445' red bed 170 8%" 2646' lime white 182 6-5/8 2801' red sdy 250 155 Table 4. sand quick lime white red sdy water 500' 520 sand quick sand gravel red sdy red quick sand red sdy gravel red red sdy red rock'W 420-455 gravel sand clay red red rock anhy red sdy salt white hd water 675' 750' sand red sharp sand red lime White sand red lime grey shale brown lime grey lime white brkn red rock lime white red rock lime white shale blue lime white shale blue lime grey lime WELL NO. 98 Cont'd. 275 285 500 510 520 575 585 400 410 415 420 455 460 465 585 610 675 750 800 845 1010 1055 1070 1105 1140 1160 1165 1190 1200 1240 1470 1480 1495 1540 shale sdy grey lime brkn grey shale blue sdy shale shale red lime shale red lime white shale blue lime grey shale blue lime white shale blue lime white shale blue lime white shale red brkn lime grey lime grey slate sdy blue shale blue cavy lime grey hard shale blue black lime lime grey TOTAL DEPTH: in hard lime. 5576' Drillers' logs of cable-tool holes - continued. 1590 1650 1640 1800 1850 1840 1920 1925 1955 1980 2080 2100 2150 2160 2190 2540 2580 2455 2700 2800 2805 5025 5050 5160 5576 /"\..a Structure contour 0 Exploration hole ~ lsol m sail .SJ,_._._- HIT zfi Contour interval 20 feet Datum mean sea level ” ' T ‘ “ ‘ """" * ““ "y “will” ... _ g _.___ 0 I - Scale --- '9, a m p C - 9., ... D . -_.. _. _, - L.,—.4 5*" ~ *5 . ,._- _“" ,_ I ~ _: ~12 i I Dicxengc _. w I . [ KENij cc. 4:4,, w I 0 WE} .7 \‘k 0 . /,“ "— A ‘\ :4. . I’ll" 5’,“ ‘ l *iaam J a _ _.—_.\g -—----.— '"Pf 3} -+ ~ \~\&*‘ . ’11,," [h f T? I II . ‘ ~ {pf 7' i.- 180 |6l lea 141 :40 j lPI '90 o I c ' O Q 4’? f?" l g 1‘7" 2389 288 73:, “_laser M" “a"? PIE, 1&7 \{i C . xi, ‘ - rim. - _ c o c " J CALT FORK 0/; 57.42.03 If/V‘LI‘; :2‘, . d; \ . i . ll N T ‘ i ”l ' .1 V k . .: A a? ‘ 7‘7 ‘58 ?95 (9 o 246 9 5 2|0If IS“; I s I 1 5 JUNE 7, :95 7‘0} Base map compiled from Texas General Land Office Maps _ TEXAS BOARD OF WATER ENGINEERS PLATE 5, - STRUCTURE MAP ON THE TOP OF THE UPPER ESKOTA GYPSUM IN PARTS 'OF STONEWALL, KENT, DICKENS, AND KING COUNTIES, TEXAS EXPLANATION /\.. Structure contour 0 Exploration hole Contour interval 20 feet Datum mean ,sea level Base map compiled from Texas General Land Office Maps _ ~ TEXAS BOARD OF WATER ENGINEERS PLATE 4—STRUCTURE MAP ON THE TOP OF THE CHILDRESS GYPSUM IN PARTS OF STONEWALL, KENT, DICKENS, AND KING COUNTIES, TEXAS - EXPLANATION W Water Table contour 0 Water well ' Exploration hole Contour interval 50 feet Datum mean sea level (lliitiy I g I :38: (;‘\ ‘\ p- DICK_§£~I§_ .99, KING_(,__3 __,_ _ -11--,..._.._.. . KENT co. STONEWALXGK , . . , I I )gwii.4 ’l'll‘vl‘. ,llllf)‘) (3 :w ()IH 'll ()IIIIII (3IIII / l p130” Y I I Base map compiled from Texas General Land Office maps TEXAS BOARD OF WA TER ENGINEERS PLATE 3 - RECONNAISSANCE MAP OF THE WATER TABLE IN PARTS OF STONEWALL, KENT, DICKENS, AND KING COUNTIES,TEXAS EXPLANATION 0 Water well ¢ Deep oil test 0 Exploration hole Contour interval |00 feet Datum mean sea level l 2 3 4 Scale L: :‘Ti,:‘—J:_‘:‘_‘_‘:_ miles ‘ I VI ‘ ' I 34. 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