Influence of Soil Conditioners on Infiltration and Water Movement in Soils1

Download Influence of Soil Conditioners on Infiltration and Water Movement in Soils1

Post on 21-Dec-2016




0 download

Embed Size (px)


<ul><li><p>Influence of Soil Conditioners on Infiltration and Water Movement in Soils1</p><p>J. W. KlJNE2</p><p>ABSTRACTThe infiltration of water at 2mbar suction into horizontal</p><p>columns of two soil materials of different textures was studied.The columns had been treated with two soil conditioners, Kriliumand poly(vinyl alcohol). The soil-water diffusivities werecalculated from the water content distribution data. Treatmentof a clay loam with the soil conditioners caused 1.5-fold to 3-foldincreases in soil-water diffusivity over the whole range ofvolumetric water contents. When expressed as a function of soilwater potential, soil-water diffusivity increased by this treatmentmore than 10-fold at the lower soil-water potentials. The sametreatment had far less effect on the soil-water diffusivity of aloamy sand. For both soils the rate of movement of the wettingfront increased as a result of treatment with the soil conditioners.</p><p>The calculated mean diffusivity and rate of movement of thewetting front in these soils was greater for n-heptane than forwater. The intrinsic diffusivity and penetrability differed forthe two permeants. Changes in viscosity, surface tension, andapparent contact angle did not account fully for this dependenceof diffusivity and penetrability on the permeating liquid.</p><p>THE FLOW OF water through soils could result from acombination of viscous movement and diffusion. Forideal porous media, the theory of these two types of movementhas been well advanced. Soil, however, does not act as anideal porous medium for water movement because of theinteraction occurring between the fluid and the medium.</p><p>The evidence obtained from studies of clay-water inter-actions (9, 11, 12) implies that adsorption and osmotic forcesmay modify the flow process through soils. Kemper (8) inattempting to evaluate the influence of osmotic forces on flowthrough soil obtained qualitative but not quantitative agree-ment between calculated and measured values of osmoticpressure. At least part of the discrepancy was attributed touncertainty in determining the average effective film thicknessfor water movement.</p><p>The influence of porosity on soil-water diffusivity wasstudied by Jackson (6) who observed that diffusivity decreasedwith decreasing porosity. It is clear that the roughness of theparticles and the actual pore geometry are also important inunsaturated water movement, but the influence of these factorsis even more difficult to assess. The contact angle in un-</p><p>saturated soil is probably not the same as would be obtainedwith the same liquid on a smooth surface. Greenland (4) has-suggested that the adsorption of uncharged polymer moleculesresults in a lining of the soil pores. This would stabilize theaggregate, but a lining of the: soil pores might also have someeffect on the flow properties through the soil. The presentstudy was initiated to investigate the influence of two differentsoil conditioners on the soil-water diffusivity in two differentlytextured soils.</p><p>EXPERIMENTAL PROCEDURELiquid flow into horizontal isoil columns was studied wi.h two</p><p>permeating liquids, a O.QIN CaSO4 solution in distilled water andw-heptane. The soil materials used were a clay loam (Urrbraered-brown earth) and a loamy sand (solodized solonetz). Thesewere used untreated or treated with Krilium (sodium salt ofhydrolysed polyacrylonitrite) or with poly (vinyl alcohol) (PVA).The treatment consisted of thoroughly stirring 100 g of air-drysoil into 25 ml of a 0.4% solution of Krilium or PVA (GohsinolGL 05, mol wt 25,000). After mixing with the soil conditioners,the soils were dried and passed through a 1-mm screen. Someof the untreated soils were mixed in the same ratio with water,dried, and sieved. The soils were then packed into clear acrylicplastic cylinders. The pressure of the liquid entering the soilcolumn was controlled by a fritted glass bead plate. The platewas filled with the permeating liquid and the desired suction(2 mbar) (15) was applied prior to placing the plate in contactwith the porous material. The suction at a; = 0, the liquid source,was precisely controlled by the use of a Mariotte bottle.</p><p> x</p><p>The columns were sectioned when the wetting front hadadvanced through the fourth of five thin (0.5-cm) sections locatednear the end of the column. Thus four water content measure-ments were obtained within 2 cm of the wetting front. Thelargest part of the fifth thin section, plus a sample from a sub-sequent 3-cm section, allowed water content measurements ot theoriginal air-dried material.</p><p>Calculations of the soil-water diffusivity were made accordingto the method developed by Bruce and Klute (1) using theequation:</p><p>D(9) == - L</p></li><li><p>KIJNE: INFLUENCE OF SOIL CONDITIONERS ON INFILTRATION</p><p>where D is the weighted-mean diffusivity (3, 6), and 0,is the watercontent at saturation.</p><p>Philip (16) proposed the term intrinsic diffusivity to denote adiffusivity which is a function of the geometry of the mediumonly and independent of the properties of the permeant. Thisintrinsic diffusivity D is related to the soil-water diffusivity by:</p><p>r , i[T cos H J D [31</p><p>where it is the viscosity, y is the surface tension, and H the angleof contact ^between the fluid and the solid. The intrinsicdiffusivity, 'S), was calculated from the weighted-mean diffusivityvalue D.</p><p>It is implied in the mathematical development of [1] that aplane of constant water content advances proportionally to thesquare root of the infiltration time. This leads to the assumptionthat the wetting front maintains a constant 8(6). [Swartzendruber(17), however, considers the Boltzmann transformation a con-sequence of the boundary conditions imposed on the problem.]Thus, a plot of the distance of the wetting front vs. x should yielda straight line through the origin. If X is the slope of this line, anintrinsic penetrability (7) can be calculated from:</p><p>[4]</p><p>where P is the intrinsic penetrability, which again is dependentonly on the geometry of the medium. Intrinsic penetrabilityvalues were calculated for the different soil materials.</p><p>RESULTSThe water-content distribution curves are shown in Fig. 1</p><p>for the Urrbrae soil samples and in Fig. 2 for the solodizedsolonetz. In order to compare the distribution curves, theexamples shown in Fig. 1 and 2 are for runs of equal lengths.The diffusivity values, however, are calculated from a largernumber of runs of different duration.</p><p>The shape of the water content distribution curves isconsiderably different for the treated and untreated samples.The water contents at x = O are increased by treatment,particularly for. the Urrbrae soil. The infiltration rates alsovary to a large extent between treated and untreated samples.Representative values of the infiltration times are given inTable 1. For each run, the diffusivity was calculated andplotted as a function of volumetric water content. Theresulting average relations are plotted in Fig. 3 and 4.</p><p>The diffusivity ranges of the individual samples at eachwater content are shown by vertical lines in Fig. 3. The</p><p>Table 1Time required for penetration of the permeating liquidinto a column of soil 20 cm long</p><p>Sample Permeant Minutes</p><p>Untreated</p><p>Krilium treatedPVA treated</p><p>UrrbraeH2OQ.QIN CaSOtn-heptaneQ.01N CaSO40.01JV CaSO4</p><p>1,3701,041</p><p>121920058</p><p> UNTREATED KRILIUM TREATED. PVA TREATED</p><p>DISTANCE FROM SOURCE (cm)15 17.5 20 22.5</p><p>Fig. 1Water content distribution curves for Urrbrae soilsamples.</p><p>0.5iHLJ 0.4O</p><p>Q:UJ</p><p>So.2</p><p>OQ.1</p><p> UNTREATED KRILIUM TREATED_._. PVA TREATED</p><p>DISTANCE FROM SOURCE (cm)2 7.5 10 125 15 17.5 20 22.5</p><p>Fig. 2Water content distribution curves for solodized solonetzsoil samples.</p><p>UntreatedKrilium treatedPVA treated</p><p>Solodized Solonetz0.017V CaSOjn-heptaneO.OlATCaSO.0.01JV CaSO4</p><p>10r64</p><p> O\ C -</p><p>E^ 1~ 0.6^ 0.4i=&gt; 0.2CO</p><p>t .06Q .04 -02&lt; .015.006^.004S.002</p><p>.001.0006.0004.0002.0001</p><p>19343</p><p>171104</p><p>HEPTANERTR:K.TR.</p><p>UNTR.</p><p>O 10 20 0/o 30 40 50</p><p>VOL. WATER CONTENT</p><p>Fig. 3Soil-water diffusivity vs. volumetric water content forUrrbrae soil samples.</p></li><li><p>10 SOIL SCI. SOC. AMEH. PEOC., VOL 31, 1967</p><p>10060</p><p>. 40i 20</p><p>1064</p><p>i 1g f f iS0-2&lt; 0.1$.06J .04S.02</p><p>.</p><p>HEPTANE</p><p>1JNTR.</p><p>K.TR.</p><p>PTR.</p><p>O 10 20 0/o 30 40 50</p><p>VOL. WATER CONTENTFig. 4Soil-water diffusivity vs. volumetric water content for</p><p>solodized solonetz soil samples.</p><p>variation is the greatest at water contents near saturation andat the lowest water contents. This variation results from thedifficulty involved in making accurate measuremtnts of dx/ddat these water content ranges, as was noted previously (7).The vaiiation between samples was about the same for bothUrrbrae and solonized solonetz samples, but for clarity thevertical lines were omitted in Fig. 4. There was no significantdifference in the diffusivity-water content relationship foruntreated samples and those which were water treated. Whenheptane was used as the permeant there was no significantdifference between untreated or Krilium- and PVA-treatedsamples.</p><p>In Table 2 are listed the weighted-mean diffusivity values(3, 5, 7) and the corresponding intrinsic values (16). Thecontact angles needed for the calculation of intrinsic values in</p><p>Table 2Values of weighted-mean diffusivity D (cm2/min) andthe corresponding intrinsic value for Urrbrae and solodized</p><p>solonetz soil samples (cm)</p><p>Sample</p><p>UntreatedKrilium treatedPVA treatedWith heptane</p><p>Weighted-meandiffusivity</p><p>D</p><p>cm2/min</p><p>Urrbrae0.260.380.474.81</p><p>Intrinsicweighted-mean</p><p>diffusivity2D</p><p>cm</p><p>3.5 X 10-=3.7 X 10-65.1 X 10-</p><p>17 X 10-8</p><p>UntreatedKrilium treatedPVA treatedWith heptane</p><p>Solodized Solonetz1.901.171.325.02</p><p>21 X10-613 X 10-13 X 10-</p><p>-17 X 10-</p><p>KRILIUMUNTR.-Q.01 N CaSO,</p><p>10 15 20 26</p><p>INFILTRATION TIMtV (min.1/2)30</p><p>Fig. 5The position of the wetting front as a function of thesquare root of the infiltration time.</p><p>equations [3] and [4] were obtained from capillary riseexperiments (10). Letey and co-workers (10) used ethylalcohol as the standard for capillary rise of a liquid with zerocontact angle for soil. However, comparison of the observedcapillary rise of ethyl alcohol and heptane into the samplesindicated that alcohol still had .a finite contact angle with soil.Therefore, heptane was chosen as the standard.</p><p>From the capillary rise of the two liquids the cosine of thecontact angle was calculated. These values and the corre-sponding angles are listed in Table 3. The differencesbetween the cosine of apparent contact angles in the untreatedsamples may appear small, but it should be noted that thesedifferences correspond to a difference of at least 5 cm incapillary rise. Each value of the cosine in Table 3 is anaverage of two or three observations. The maximum differencein capillary rise between replicates was 1 cm.</p><p>Figure 5 shows the position of the wetting front as afunction of the square root of the infiltration time for anumber of runs with Urrbrae samples. The lower curve foruntreated soil in Fig. 5 was obtained from the infiltration ofdistilled water into the column. With this sample a smalldeviation from linearity was observed (2) which probablyresulted from slight swelling of the sample. From the slope,X, of curves like those in Fig. i), intrinsic penetrabilities werecalculated. These data are given in Table 4. The rate ofmovement of the wetting front with heptane as the permeantwas not significantly affected by treatment and therefore onlyone value was listed in Table 4.</p><p>Table 3Contact angles for water infiltration from capillary riseexperiments</p><p>Sample </p><p>UntreatedKrilium treatedPVA treated</p><p>Contact angle</p><p>Urrbrae80" 1376 4377 53</p><p>Cosine</p><p></p><p>UntreatedKrilium treatedPVA treated</p><p>Solodized Solonetz78 1079 376 7</p><p>0.2050.190.24</p></li><li><p>KIJNE: INFLUENCE OF SOIL CONDITIONERS ON INFILTRATION 11</p><p> URBRRAE--SOL. SOLO METZ</p><p>-12 -10 -8 -6 -4 -2 (TSOIL-WATER POTENTIAL (atm.)</p><p>Fig. 6Soil-water diffusivity as a functon of soil-water potential.</p><p>DISCUSSIONSoil-Water Diffusivity</p><p>Treatment of Urrbrae soil samples with either Krilium orPVA markedly increased the soil-water diffusivity of this soilover the whole range of volumetric water contents (Fig. 3).Both these materials are known to have a stabilizing influenceon the soil structure. Hence, it was expected that the waterconducting qualities would be improved by treatment. Thiswas confirmed both by the shape of the water contentdistribution curves and the infiltration rates.</p><p>The water content distribution curve is determined by thediffusivity at relatively low water content. This is particularlyapparent from Fig. 7 where the water content distributionpresented results from infiltration of distilled water and theQ.QIN CaSC&gt;4 solution into untreated Urrbrae soil. Thederived diffusivity-water content relationship is given in thesame figure. The infiltration of the CaSOi solution results ina steep slope near the wetting front in the water content</p><p>Table 4Values of X and intrinsic penetrabilities for Urrbraeand solodized solonetz soil samples</p><p>Sample for 0.01N forCaS04 n-heptane</p><p>Intrinsic penetrabilityfor0.01Ar for</p><p>CaSOi n-heptane</p><p>UntreatedKrilium treatedPVA treated</p><p>Jcm/min</p><p>Urrbrae0.62 1.810.660.78</p><p>cm</p><p>23 X 10-'21 X 10-'26 X 10-'</p><p>33 X 10-'</p><p>Solodized SolonetzUntreatedKrilium treatedPVA treated</p><p>1.441.531.56</p><p>3.06 48 X 10-' 56 X 10-*52 X 10-'48 X 10-'</p><p>5 10DISTANCE</p><p>FROM SOURCE (cm)</p><p>20 0-1 02Q</p><p>Fig. 7Water content distribution curve and the correspondingsoil-water diffusivity relationship for untreated Urrbrae samplesinfiltrated with water and 0.01N CaSO4 solution.</p><p>distribution curve. Thus, the area under the curve is largerfor CaS04 than for water. This corresponds to lower diffusiv-ity values for the CaS04 run at low water contents. The highdiffusivity values for a CaSCh solution at water contents above22% result in a higher infiltration rate for CaSC&gt;4 solutionsthan for distilled water (Fig. 5). This is in agreement withthe observation of Hanks and Bowers (5) that the infiltrationrates are determined more by the diffusivities at the higherwater contents than by those at lower water contents.</p><p>The same principles hold for the infiltration of the solutioninto the differently treated soils. For example, the area underthe water content distribution curve for PVA-treated Urrbraeis larger than for Krilium-treated Urrbrae, whereas thediffusivity values for PVA-treated Urrbrae are less than thosefor Krilium-treated Urrbrae below a water content of 30%.The water contents near the liquid source, at a; =0, aredifferent for the different treatments and this influences thearea under the water content distribution curve. However,the diffusivity for untreated Urrbrae is less than for Krilium-treated Urrbrae, even at low water contents, although thearea under the water content distribution curve for Krilium-treated soil is larger. This results from the dominatinginfluence of the low infiltration rate into untreated Urrbrae(Table land Fig. 5).</p><p>In the case of solodized solonetz (Fig. 2 and 4) the generalpicture is somewhat different since treatment with Kriliumand PVA reduces the soil-water diffusivity. This is particularlyapparent for the lower soil water contents. There is againconsistency between high values of diffusivity...</p></li></ul>


View more >