J 
 
LIBRARY 
 
 UNIVE»SITY OF CALIFORNI>» 
 DAVIS 
 
 A^. 
 
APPENDIX E 
 
 PRELIMINARY CHEMICAL QUALITY STUDY IN 
 THE MANHATTAN BEACH AREA, CALIFORNIA 
 
 United States Geological Survey- 
 Water Resources Division 
 Quality of VJater Branch 
 
UNITED STATES 
 
 DEPARTMENT OF THE INTERIOR 
 
 GEOLOGICAL SURVEY 
 
 Quality of Water Branch 
 
 PRELIMINARY CHEMICAL- QUALITY STUDY IN THE 
 MANHATTAN BEACH AREA, CALIFORNIA 
 
 By Robert Brennein 
 
 Prepared in cooperation with the California 
 Department of Water Resources 
 
 Sacramento, California 
 Axigust, 1956 
 
CONTENTS 
 
 Page 
 
 Introduction 2 
 
 Acknowledgments 9 
 
 Description of the area 9 
 
 Chemical relations in the water 15 
 
 Summary 32 
 
 References 3^ 
 
 ILLUSTRATIONS 
 
 Figure 1 Location of wells in the Manhattan Beach project area, 
 
 Manhattan Beach, California 4 
 
 2 Geologic profile through the "C" line of wells showing 
 the extent of the Silverado water-bearing zone and 
 variation of chloride and total hardness with sampling 
 
 depth 11 
 
 3 Geologic profile through the "G" line of wells showing 
 the extent of the Silverado water-bearing zone and 
 variation of chloride and total hardness with sampling 
 
 depth 12 
 
 ^4- Geologic profile through the "K" line of wells showing 
 the extent of the Silverado water-bearing zone and 
 variation of chloride and total hardness with sampling 
 depth 13 
 
 5 Water-level contours for 1903-0^+ and I9U5 in the 
 
 Manhattan Beach area ih 
 
 6 Trilinear plot of selected analyses from the Manhattan 
 
 Beach area -^-T 
 
 7 Calcium, magnesium, and chloride concentrations in the 
 leach of core material from the Silverado water-bearing 
 
 zone with a sodium chloride solution and sea water 19 
 
 TABLES 
 
 Table 1 Mineral constituents and related physical measurements 
 of the ground water of the Silverado water-bearing zone 
 in the Manhattan Beach area, selected samples of oil 
 field brines and ocean water, CaJ.ifornia 5 
 
 2 CsLlculated mixtures of native water with ocean water 
 and oil field brines for selected analyses from the 
 
 mxmicipal well 8, Manhattan Beach, California 22 
 
 3 Calculated mixtures of native water and ocean water for 
 selected analyses from the "C" line of wells, Manhattan 
 
 Beach, California 26 
 
 k Calculated mixtures of native water and ocean water for 
 selected analyses from the "G" line of wells, Meinhattan 
 
 Beach, California 27 
 
 5 Calculated mixtures of native water and ocean water for 
 selected analyses from the "K" line of wells, Manhattan 
 Beach, California 28 
 
 -1- 
 
PRELIMINARY CHH-IICAL- uALITY STUDY IN THE 
 MANHATTAN BEACH AREA, CALIFORNIA 
 
 ' 5 
 
 By 
 
 Robert Brennan 
 
 INTRODUCTION 
 
 In 19011. Mendenhall (1905) made a survey of the ground water 
 conditions in southern California. At the time of his survey the 
 piezoraetric surface in the area was above sea level, but since that time 
 water levels have declined. During the 1920' s, years of rapid development, 
 the water levels declined at an increasing rate • However, because of 
 decreased pumping during the depression years of the 1930' s, the levels 
 tended to recover somewhat. During the war years of the 19U0's, a large 
 expansion of industry occurred in the area, and ground water withdrawals 
 greatly increased. By 19ii5 water levels in some areas had declined as 
 much as 70 feet below sea levels In the coastal region this heavy with- 
 drawal and the ensuing dry years rapidly lowered the ground water levels, 
 reversing the normal seaward flow of the underground water to a landward 
 flow. 
 
 In 19hO a definite increase in the salinity of the ground water 
 was noticed at the i-ianhattan Beach municipal well field. The salinity 
 increased over the years until most of the original wells of the field 
 had to be abandoned. In 19U7 Poland, Garrett, and others (1959) made 
 studies of the contamination of the ground water in the Manhattan Beach 
 area and concluded that the contairdnating agent was most likely ocean 
 water. 
 
 -2- 
 
The State of California with its many coastal basins has been 
 most conscious of the value of its ground-water supplies. The possibility 
 of sea-water encroachment into these underground reservoirs has been recog- 
 nized, and means to prevent it have been and still are being sought. In 
 1950 the California State Legislature appropriated $700,000 for the 
 experimental work connected with the study of this problem. The Manhattan 
 Beach area was selected as the site for experiments to study the feasi- 
 bility of creating a fresh-water barrier close to the coast to prevent 
 sea-water encroachment. The work of this project was carried out by the 
 Los Angeles County Flood Control District under contract with the State 
 Water Reso-orces Board and under the supervision of the California Division 
 of Water Resources. 
 
 The study involved the injection of Colorado River water from 
 the Metropolitan Water District into a line of wells roughly parallel to 
 the coast and tapping only the main confined aquifer, thereby building 
 up a "pressure ridge". In the course of this workj nine 12-inch injection 
 vrells and thirty-six S-inch observation wells were drilled. Figure 1 is 
 a map of the area showing the location of the wells. 
 
 As a part of this investigation,, I66 samples of the ground 
 water were obtained from the wells prior to the injection of the fresh 
 water and were analyzed by the Uo S. Geological Survey. In addition, as 
 each well was developed chloride, conductance, and density determinations 
 were made in the field by the Los Angeles County Flood Control District. 
 Many analyses of water from the Manhattan Beach municipal wells also were 
 available. Table 1 presents the analyses of the ground water of the area 
 and selected analyses of ocean water and oil-field brines. 
 
LEGEND 
 
 Figure I — Location of wells in the Manhattan Beach Project, 
 Manhattan Beach, California 
 
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From geologic and hydrologic evidence it was concluded by Poland 
 and others (1959) that ocean water was encroaching into the v/ater-bearing 
 zone in the Manhattan Beach area^ and model studies have been made at the 
 University of California. Experimental Station^ Richmond,, California, which 
 show that the encroaching water probably enters the zone in the shape of 
 a wedge. It is the purpose of this report to review the chemical-quality 
 data obtained in the Manhattan Beach area and to determine whether these 
 data lend support to these conclusions, 
 
 ACKMOWLEDGMENTS 
 
 The study described in this report was made by the United States 
 Geolcgical Survey at the request of and in cooperation with the California 
 State Department of Water Resources. It was under the supervision of lo W„ 
 Wallingj District Chemist^ Sacramento^, California, 
 
 Water samples analyzed by the U.S. Geolcgical Survey were col- 
 lected by personnel of the California State Department of Water Resources 
 and Los Angeles Coijmty Flood Control District, 
 
 Density;, conductaneej and chloride data made in the field by 
 the Lcs Angeles County Flood Control Distiict and well logs were supplied 
 by the California State Department of Water Resources, 
 
 DESCRIPTION OF THE AREA 
 
 The hydrologic data for this section of the report as well as 
 Figure 5 have been abstracted from the report by Poland (1959) on this 
 area. 
 
 The Manhattan Beach area discussed in this report lies vrithin 
 the West Basin in Los Angeles County, The principal aquifer^ known as the 
 
Silverado water-bearing zone, is composed of sandy and gravelly phases 
 of beach and marine deposits of Pleistocene age. Except in the reaches 
 adjacent to the present shoreline, this aquifer is confined under artesian 
 pressure in the Manhattan Beach area,, The confining bed consists of clay 
 on top of the aquifer. The aquifer also is underlain by clay. The 
 Silverado zone is said to be "merged" in this area because the several 
 distinct aquifers present in the zone inland have converged to form a 
 single aquifer in hydrologic continuity m.th the inland aquifers. 
 Figures 2 5 3^ and I4 show the extent of the Silverado zone in the report 
 area. 
 
 Recharge of fresh water into this aquifer comes mainly from 
 the intake areas inland frdm the Newport-Inglewood uplift^, but some local 
 penetration of rainfall also recharges the aquifer. 
 
 The Newport-Inglewood fault zone, which forms the eastern 
 edge of the West Basin^ acts as a partial barrier to fresh-water recharge 
 to the aquifer. Loxrering the piezometric surface west of the faults will 
 increase the flow across the faults j and conversely ^ lowering the 
 piezometric surface east of the faults will reduce the recharge to the 
 West Basin. 
 
 At the time of Mendenhall's work the water level in the 
 ViTest Basin was above sea level and that east of the fault zcne was still 
 higher. The ground water flowed across this fault zone and discharged 
 into the ocean. Figure ^ shows the water level for 1903~Oli from the data 
 of Mendenhall as modified by Poland, Since the time of I-iendenhall's workj 
 withdrawal of the ground water in the West Basin has increased, and the 
 water level has declined as shown by the water level in the area for 19h$ 
 (Figure 5). The recharge of fresh water across the Newport-Inglewood 
 
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Figure 3 — Geologic profile through the "G" line of wells showing the extent of the Silverado 
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Figure 5 -- Depth to water for 1903-04 and 1945 in the 
 
 Manhattan Beach Area, California 
 
fault zone also has decreased, owing to the lowering of the water level inland 
 from the faults. A depression in the piezometric surface has formed in the 
 West Basin east of the Manhattan Beach area. This depression inland from the 
 ocean has reversed the normal seaward gradient in the coastal area and allowed 
 sea water to more inland. 
 
 CHEMICAL RELATIONS IN THE WATER 
 The earliest chemical-quality data available for the ground water in 
 the Manhattan Beach area are from the Manhattan Beach municipal well field. 
 These analyses show that the water as of 1938 was of the calcium and magnesium 
 bicarbonate type. In this report the analysis of the water from the Manhattan 
 Beach municipal well 8 for October 1938 is considered as water native to the 
 Silverado water-bearing zone prior to the present saline contamination. The 
 concentrations of the ions in this water are used in all calculations involving 
 native water. It is not to be construed that the concentration of a single 
 analysis adequately represents all the water of the aquiferj however, large 
 errors will not be introduced by using a single analysis because, generally, 
 the chemical quality of ground water at a selected sampling point does not undergo 
 marked changes with time unless contaminated, and the total dissolved mineral 
 concentration of the native water is very small compared to the saline"-c.pntaminant 
 in this area. 
 
 The word contamination is used in this report in the broad sense to 
 cover deterioration in chemical character of the water without regard to 
 concentration or source of the contamination. This broad usage should not be 
 confused with the established usage of the word in the California Water Code 
 (Water Code of 19U9, Division 7, Chapter 2, Definitions). 
 
 Figure 6 is a trilinear plot of selected analyses of the ground water 
 from the Manhattan Beach area. This plot shows the changes in chemical 
 
 -15- 
 
character of the ground water in the area from 1938 to 1953 and also the change 
 in character of the water coastward from the Manhattan Beach mimicipal well 
 field o Hie principles involved and the procedures used in plotting the 
 chemical character of waters on this type of plot have been described by 
 Piper (I9ii5). 
 
 Chemical data for the water of the municipal well field in 1938 
 plots just to the left of center in the central diamond of the figure, and 
 later analyses of water from the same well plot away from the native water 
 approximately in a straight line and toward the top of the diamonds The 
 total dissolved mineral content of the water has increased and the percentage 
 concentration of the ions expressed in equivalents per million has changed « 
 Percentage changes in the cations of analyses 1 through 10 shown in the left- 
 hand triangle have been small. The calcium and magnesium have increased by 
 approximately 10 percent and the percent sodium has decreased by an equal 
 amount. The anion percentages, as shown in the right-hand triangle, have 
 undergone large changes. The bicarbonate-type water originally present has 
 progressively changed to a chloride-type water. The sulfate percentage has 
 remained relatively constant, producirig a straight-line plot in the triangle. 
 Plotting analyses of water from project wells closer to the ocean produces a 
 new plot in the diamond. These analyses plot in a line along the edge of the 
 diamond, descending downward from the apex to a point which represents essentially 
 undiluted sea water. Generally, as the locations of the wells approach the 
 ocean, the analyses of these well waters approach that of sea water. 
 
 -16- 
 
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Simple mixing of the native water with sea water or an oil-field 
 brine vrould give a series of plots approximatinp; a strair^ht line .ioininp 
 the native water and the sea water or brine. Obviously, simple mixing of 
 sea vfater or a brine with the native vrater has not taken place. No single 
 type of water vjill produce a (louble-line plot such as this by simple 
 
 admixture of tv/o vraters. The chemical change may be that of cation 
 exchange. This ty|)e of change requires that ion-exchange materials bo 
 present in the Silverado zoneo 
 
 Several core samples of the Silverado water-bearing zone were 
 obtained from wells 11-I8 and H-I6 and tested for exchange materials. The 
 sediment samples were obtained from three different depths in each vrell 
 and thoroughly mixed » The dry material was placed in a column and Icachod 
 Tifith distilled water until most of the soluble material was removed, as 
 indicated by a decrease in hardness of the leachate to 100 opiu, a liter 
 of sodium chloride solution of approximately the concentration of sea 
 water was introduced i.nto the coliamxio lihcn the silver nitrate test indicated 
 tho orcsencc of chloride in the leach, samples 1 • i^ve collected and 
 analyzed for calcium, magnesium, and chloride. iJ'igure 7a siovis the results 
 of these analyses. .aximum ion exchange apparently took place in about two 
 hours and then steadily decreased '.irith time. The maxiii:;um exchange noted 
 (between 9 and 11 hours) was slightly less than the concentration of sodium 
 in the solution addedo 
 
 The core material was regenerated with a calcium ciJ.uri'Jij 
 solution and again rinsed i/ith distilled vjabor unt i rinse showed n 
 total hardness of approximately 100 npiri. .'. litni- - ' I. ;cn 
 
 introduced at the top of the column and samples of leach collected and 
 
 -18- 
 
lAJUUL 
 
 Calcium 
 Magnaiiu n 
 
 i ^ 1^ 
 
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 Sompling timt in hour* 
 
 Figure a — Calcium, magnesium, and chloride concentrotlons in the leoch from the Silverodo water- bearing zone 
 
 core motenol leached with a sodium chloride solution 
 
 ^00 
 
 /< Chlorid» 
 
 / 15.000 
 
 200 
 
 
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 Calcium 
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 Sampling ttmt in houri 
 
 Figure b — Calcium, mognetium, and chloride concentrotiont in the leach from the Silverado water-bearing 
 
 zone core materiol Itachtd with sto water 
 
analyzed as before. The flow through was faster during this second run. 
 Figure 7b shows the results of these analyses. As with the sodii:m chloride 
 solution, ion exchange took place rapidly increasing to a maximum and then 
 decreasing. After about five hours, the leach attained a calcium and 
 raagnesium concentration of the sea xrater added. Because the column was 
 regenerated with a calcium chloride solution, it should not be inferred 
 from the sea-water data that the magnesium of the sea water exchanges for 
 the calcium of the soil. This aspect of ion exchange was not investi- 
 gatedj only the possibility of ion exchange was sought. The postulation 
 that ion exchange is the mechanism by which the observed chemical 
 phenomena can be exolained is supported by these tests showing that 
 minerals capable of entering into ion-exchange reactions are present in 
 the Silverado water-bearing zone. 
 
 The double-line plot of the trilinear diagram can be explained 
 on the basis of ion exchange coupled with simple mixture. The contaminating 
 water, as it moves through the Silverado zone, undergoes cation exchange. 
 In the resulting mixture of native and contaminating water the percentage of 
 calciiim plus magnesiiim wi-11 remain constant or increase to a maximum if the 
 inflow of contaminating water steadily increases. When this maximum point 
 is reached, the high sodium content of the contaminating water causes the 
 percentage of sodium to increase in the mixture until the contaminating water 
 constitutes 100 per cent of the mixture. 
 
 Sea water and oil-field brines are two possible sources of 
 contamination in the Manhattan Beach area. Hydrologic evidence favors sea 
 water, and if this is valid, chemical-quality data also should support this 
 conclusion. 
 
 -20- 
 
There are oil wells north, west, and southwest of the Manhattan 
 Beach area. Samples of brines from these fields (Table l) are lower in 
 sulfate and higher in carbonate than sea v/ater and plot below sea water in 
 the trilinear diagram. 
 
 Selected analyses from the Manhattan Beach municipal well eight 
 were compared with hypothetical mixtures of native water and sea water 
 and native vjater and oil-field brines. These hypothetical mixtures were 
 calculated by determining the percentages of contaminating water and 
 native water required to produce a water whose chloride content in 
 equivalents was equal to the equivalents of chloride of the water actually 
 analyzed. Table 2 compares the analyses with the hypothetical mixtures 
 of native water with sea water and oil-field brines. 
 
 These data show that the sum of the equivalents of calcium and 
 magnesium in the natural well water exceeds the sum of these ions in the 
 hypothetical mixtures, and this difference increases as the total dissolved 
 mineral concentration increases. Similarly, the equivalents of sodium in 
 the natural well water is less than the equivalents of sodium in the 
 hypothetical mixt\ires in all instances, and this difference is approxi- 
 mately equal to that for the calcium and magnesium. This indicates that 
 ion exchange has taken place as well as simple mixture. 
 
 The hypothetical mixtures of sea water and native water indicate 
 that the loss of sodium and potassium ions is slightly larger than the 
 gain of the calcium and magnesium ions and that this difference is equal 
 to the loss of the anions bicarbonate and sulfate. This loss can be 
 explained as precipitation of salts from solution. If the sodium ions of 
 sea water exchange for calcium, barium, strontium, etc, of the soil and 
 any of the ions later precipitate from solution as the carbonates or 
 sulfates, the apparent loss would be in sodium carbonate and sulfate. 
 
 -21- 
 
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The hypothetical mixtures of native water and brine indicate 
 that the gain of the alkaline -earth ion is larger than the loss of alkali 
 ions and that the difference is almost equal to the gain of sulfate ions. 
 The solution of calcium sulfate from gypsum deposits in the Silverado 
 zone would provide an explanation of this gain. That this has not been the 
 case is evidenced by the net loss of sodium carbonate in the less contami- 
 nated water and not a gain of calcium sulfate, and by the low sulfate 
 concentration in the native water. This would not be expected if gypsum 
 deposits were common in the Silverado zone. For this reason sea water 
 seems the more logical contaminating agent. 
 
 The project wells, which are nearer the ocean than vjell eight, 
 yield more highly concentrated water than do wells farther away. The 
 selected analyses plotted In I'lj^ure 6 shovj that sea-water character is 
 approached with decreasinp dintnnce from the well to the ocean. Analyses 
 A and B are from waters in wells that tap the Silverado zone in the area 
 between the Manhattan Beach municipal well field and the Rosecrans and 
 Torrance oil fields. 
 
 These analyses do not show increased contamination and, in fact, 
 are similar to native water in concentration and character. This gives 
 further indication that in the I'^anhattan Beach area sea v/ater is the saline 
 contaminant , 
 
 The ratio of chloride to bromide also f;ives evidence that the 
 contaiainant is sea water. The ratio of chloride to bromide in sea water 
 is about 290 to 1. Host of the water samples collected in the Manhattan 
 Beach area have a chloride-to-bromide ratio between 270 and 310 to 1, The 
 less concentrated waters shov; larger deviations from the sea-water ratio. 
 This probably is due mainly to the error of the bromide determination. In 
 
 -23- 
 
the waters of lo\'j concentration the relative error is larger than in those 
 of high concentration. 
 
 A review of the manganese content of the waters introduces some 
 interesting facts. The greatest concentration of manganese is found in 
 waters from wells along the injection line and just inland from this line 
 in the vicinity of the "G" injection well. The manganese content decreases 
 seaward and landward from this line of high concentration. Generally, the 
 manganese content increases with depth within a particular well. 
 
 This increase in manganese content probably is brought about 
 by ion-exchange phenomena. The sodium ions of the sea water are exchanging 
 for manganese ions in the materials of the Silverado zone. The greatest 
 manganese concentration seems to occur when the magnesium content is equal 
 to or just exceeds the calcium content. 
 
 Sea-water contamination of fresh-water bodies is not unique to 
 California. Many coastal areas and island provinces have the same problem. 
 In working vjith these problems over the years, hydrologic data have shox-m 
 that the heavier sea water enters an aquifer at the bottom and does not 
 mix completely. Some island countries obtain fresh water which overlies 
 sea water and, if the pumping is not too heavy, contamination can be 
 prevented. 
 
 As a part of the study of the Manhattan Beach project a model 
 of a confined aquifer was built by the University of California Experimental 
 Station at Richmond to furnish hydrologic data for a body of sea water 
 trapped inland from the injection line as a fresh-water pressure ridge was 
 being built up. In addition to these data, the model studies also showed 
 that the sea water first would enter the basal deposits of the aquifer and 
 then advance inland as a sloping wedge until it completely filled the 
 
 -2k- 
 
confined zone. Project wells situated in the frontal portion of the 
 intruding sea water provided sampling opportunities v/hich aided in the 
 proof of the viedge theory^ 
 
 Three concepts can be postulated about the behavior of a vredge 
 of saline water moving against a body of fresh vrater in an aquifer; 
 (l) The depth to sea water below a horizontal plane should be less near 
 the coast than inland; (2) any fresh vjater remaining in the aquifer will 
 be found in the uppermost oart of the aquifer j and (3) a zone of mixed 
 sea vjater and fresh v/ater should be encountered at the sea water-fresh 
 water interface. 
 
 To obtain the best data on the shape and extent of the intruded 
 body of sea water a static situation would be desirable. However, in 
 practice this is impossible to attain, because pumping the wells disturbs 
 the balance between the saline water and the fresh water causing the 
 waters to mix. Pumping also disturbs the rate of movement of the wedge 
 in the vicinity of the well. 
 
 Samples of water were collected from the many project vrells 
 at different depths as they v;ere developed. These data lend themselves 
 to some proof of the wedge concept. Three lines of observation v/ells 
 were drilled roughly perpendicular to the line of injection wells and 
 extending inland from the coast about half a mile. Figures 2, 3, and 1; 
 shov; the chloride content and total hardness of selected samples from the 
 "C", "G% and "K=' lines of wells as of February, 1953. The vjater from the 
 more inland vfells had lov;er chloride concentration and the concentration 
 increased with depth in any particular v;ell. The relative amounts of 
 hardness increased inland, indicating greater ion exchange at the saline 
 front, ViHiere the aquifer v/as saturated with sea water, the ion-exchange 
 
 -25- 
 
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capacity of the materials was exceeded and no further evidence of ion 
 exchange was apparent. 
 
 Tables 3, h, and 5 present the chemical analyses for the water 
 samples from the several wells and the hypothetical mixtures of native 
 water and sea water having the same chloride content. The analyses from 
 the "C" line of wells show that the water from wells C-9, C-5, and C 
 was essentially sea water. The water from well C~k at 77 feet below sea 
 level was approximately 87 per cent sea water with greater hardness 
 than the more seaward wells. The water from 53 feet below sea level 
 vjas approximately 68 per cent sea water and had a slightly higher hard- 
 ness. Further inland at well C-8 the water from Ii7 feet below sea level 
 was less than twice as concentrated as the designated native water, where- 
 as the water from 95 feet below sea level xras about 76 per cent sea water. 
 The water from $2 feet below sea level in well C-12 ^^ras less concen- 
 trated than the dilute water from well C-8 and the water from 92 feet below 
 sea level was only 36 per cent sea vrater compared to 68 per cent for water 
 at that depth in well C-8. The calcium and magnesium percentage increased 
 markedly in the water from well C-12. 
 
 The analyses of the water from the "G" line of wells show that 
 the aquifer inland to v;ell G-5 was essentially sea water for the total 
 thickness. The water at 71 feet below sea level from well G-3 v:as about 92 
 per cent sea water but water from 123 feet below sea level was essentially 
 sea water. The water at 76 feet belo^^^ sea level from well G-1 was about 90 
 per cent sea water and showed increased hardness. A water sample from hS 
 feet below sea level in well G-2 was approximately 38 per cent sea water 
 and relatively high in hardness, whereas the water from 66 feet below sea 
 level was about 86 per cent sea vrater and exhibited a smaller percentage 
 
 -29- 
 
of calcixim and magnesium. Water from 30 feet below sea level in well G-U 
 was approximately three times as concentrated as native water but at 73 
 feet below sea level the water was 80 per cent sea water. Water at 105 
 feet belovi sea level in well G-l; was essentially sea water o 
 
 Water from U8 feet below sea level in well G-8 was approximately 
 the same as water from 30 feet below sea level from well G-I4.. The water 
 at 86 feet below sea leA^el in well G-8 showed increased concentration 
 with continued pumping. After four hours of pumping the water vjas about 
 12 per cent sea water, but after 20.5 hours it increased to 2? per cento 
 This illustrates the change in the rate of movement of the saline water 
 under conditions of p'omping. 
 
 The analyses of the water from the "K" line of wells show that 
 the water in wells K-9 and K-5 was essentially sea water. The water from 
 UO feet below sea level in well K-5 was only 8? per cent sea water, 
 indicating that the aquifer was not completely filled with sea water in 
 the total thickness of the aquifer. The analysis of water from well "K" 
 was obtained from 2hS feet below sea level. This is apparently below 
 the base of the Silverado water-bearing zone, and the mixture of water 
 from the Silverado zone and a deeper, relatively uncontaminated aquifer 
 probably accounts for the lower concentration. No water samples were 
 obtained at lesser depths from this well. 
 
 The water from well K-I4 at $0 feet below sea level was about 
 67 per cent sea water whereas the water from depth 69 feet below sea 
 level was 89 per cent sea water. The relative hardness was greater in 
 the less concentrated water at shallow depth. At 77 feet below sea level 
 in well K-8 the water vras 68 per cent sea water but at 90 feet below sea 
 
 -30- 
 
level the water was 75 per cent sea water. The relative hardness of these 
 waters was higher than for the waters from well K-U and decreased with 
 depth within the well. 
 
 The vjater from vfell K-12 at 06 feet below sea level came 
 from the "200-foot sand", and was essentially native water. The upper 
 water-bearing zone in Figure h is the "200-foot sand" which merges with 
 the Silverado zone near the coast to form the single merged Silverado 
 water-bearing zoneo The water from 85 feet below sea level was obtained 
 from the Silverado zone and ivras 28 per cent sea water. The relative 
 hardness of this water was very high. 
 
 The analyses of water from well K-l6 seem to show rather 
 anomalous results. The water at 78 feet below sea level was about 10 
 per cent sea water whereas the water from 128 feet belovj sea level was only 
 about tvjice the concentration of native water. The cause of this anomaly 
 is not knovm. 
 
 The vjater samples collected from the wells in the "G", "G", and 
 "K" lines show to a large extent that chemical-quality data do substantiate 
 the hydrologic conclusions of an advancing wedge of saline water into the 
 confined aquifer. More complete sampling in wells farther inland un- 
 doubtedly vrould provide better evidence of the existence of a saline wedge. 
 
 ■31- 
 
SUMI4ARY 
 
 Years of decreased rainfall and increased ground-water use 
 have brought about a rapid lowering of ground-water levels in the West 
 Basin of Los Angeles County. The lowering of water levels has reversed 
 the normal seaward gradient of the ground water to a landward gradient 
 in the VJest Basin thereby allowing sea water to encroach into the ground- 
 water reservoir. In 1950 the California State Legislature appropriated 
 $750^000 for the study of means to prevent sea-water encroachment of 
 ground-water basins. The Manhattan Beach area was selected as the site 
 to study the feasibility of creating a pressure ridge of fresh water near 
 the coast to hold back the sea water. 
 
 The chemical -quality data obtained from the project wells have 
 been reviewed and interpreted. These data support the previous con- 
 clusions made from hydrologic evidence that sea water is the contaminant 
 and that the relatively dense sea water will enter a zone in the shape 
 of an advancing vjedge. 
 
 Chemical-quality data from the Manhattan Beach municipal 
 well eight indicate that the concentration of dissolved minerals in the 
 water has increased over the years and that the chemical character of 
 this water has approached the character of sea water. Comparison of the 
 contaminated water with hypothetical mixtures of sea water and native 
 water indicate that simple mixing has not taken place but that the 
 sodiijim ions in the sea water have probably been exchanged for the calciiun 
 and magnesium in the sediments. The calcium and magnesium percentages 
 are higher and the sodium percentage is lower than would be expected from 
 simple mixture of native fresh water and sea water. 
 
 •32- 
 
Core samples of material from the Silverado water-bearing zone 
 v;ere obtained and leached with a sodium chloride solution approximately the 
 concentration of sea water and with a sample of sea water. These data show 
 that minerals capable of entering into ion exchange reactions occur in the 
 Silverado zone. Analyses of water from wells close to the ocean and oil 
 fields show that contamination increases in the direction of the ocean and 
 not in the direction of the oil fields, thereby substantiating other 
 observations that the source of contamination is sea water. 
 
 Chemical-quality data of waters from wells normal to the coast 
 show that the contamination increases with depth in the vrell. In most 
 places essentially native fresh water was found in the upper part of the 
 aquifer. The depth to the saline water body increased with increasing 
 distance inland. This increase in deoth to the saline water body in a 
 landward direction indicates that saline water ;-7as entering the aquifer 
 in the shape of a sloping wedge. 
 
 The chemical-quality data obtained in the Manhattan Beach area 
 substantiate the previous conclusions of encroaching sea water and lend 
 support to the hypothesis that sea water will enter a confined zone as an 
 advancing wedge. 
 
 -33- 
 
REFERENCES 
 
 Mendenhall, W. C, 1905, Development of underground waters in the western 
 coastal plain region of southern California: U. S. Geological 
 Survey Water-Supply Paper 193. 
 
 Piper, A, M., 19^5, A graphical procedure in the Geochemical interpre- 
 tation of water analyses: Trans. Am. Geophysical Union, I9I4.U, 
 pt. 6, p 91U-923. 
 
 Poland, J. F., Garrett, A. A., and Sinnott, Allen, (1959), Geology, 
 hydrology, and chemical character of the ground waters in the 
 Torrance - Santa Monica Area, Los Angeles County, California: 
 U„ So Geological Survey Water-Supply Paper lit6l. 
 
 -31^- 
 
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