ll”NIH!llHlllll‘llllllHllHlllllHlIHHIIHWII lllHlli I | .THS_ IHESlS LIBRARY Michigan Sta :9 University This is to certify that the thesis entitled Relating Soil Wetness to Selected Soil Properties presented by Magdal Nawaf Haji has been accepted towards fulfillment of the requirements for M.S. Crop & Soil Sciences degree in ((22110)! / ”70427971 5. Major professor Date August 23, 1984 0-7639 MSU is an Affirmative Action/Equal Opportunity Institution )V1531_) RETURNING MATERIALS: Place in book drop to LJBRARJES remove this checkout from 4--3--_ your record. FINES will be charged if book is returned after the date stamped below. RELATING SOIL WETNESS TO SELECTED SOIL PROPERTIES By Magdal Nawaf Haji A THESIS Submitted to Michigan State University in partial fulfillment of the requirements for the degree of MASTER OF SCIENCE Department of Crop and Soil Sciences 1984 ABSTRACT RELATING SOIL WETNESS TO SELECTED SOIL PROPERTIES By Magdal Nawaf Haji Soil morphological features, particularly soil color are a key for the inference of depth to a sea- sonally high water table. Depths to saturated zones were monitored over a 4—year period on three hydrosequences. Water contents (Z by volume) were measured biweekly using a neutron moisture meter. These measurements were compared with water contents of undisturbed cores for the same depths to determine the saturated zone. Soil temperatures at 30, 50, 60, and 90 cm were measured biweekly. A set of criteria relating soil color with depth and duration of the saturated zone was found in this study of loamy soils. Horizons that have a matrix color with a chroma of 4 or more are never saturated if gray argillans and mottles are absent, but are saturated for 14-16 weeks if faint mottles and gray argillans are present. Horizons that have a matrix color with a chroma 3 are saturated for 12-14 weeks if gray argillans or some faint mottles or both are present. Horizons that have a matrix color with a chroma 2 are saturated for 22-24 weeks if gray argillans and non gray mottles are present. Horizons that have a matrix color with a chroma of 1 are saturated for 26-28 weeks if distinct and prominent mottles are present. Horizons that have matrix colors with a chroma of O with distinct or prominent mottles or both are saturated for more than 32 weeks. This study suggests that soils with horizons having a 3 chroma matrix with mottles and/or gray argillans are aquic intergrades. ACKNOWLEDGEMENTS I wish to express my gratitude to Dr. D.L. Mokma, my major advisor, for the guidance, and friendship given to me during my M.S. program in the Department of Crop and Soil Sciences at Michigan State University. Gratitude is also due to those who served on my graduate committee, Drs. G.J. Larson and R.J. Kunze for their valuable suggestions and professional instructions. I wish to extend my appreciations to my family for their support and encourgement during my study. iii 10. TABLE OF CONTENTS Page List of Tables... .......................... V List of Figures................. ........... Vi Introduction....... ..................... ... 1 Literature Review.. .................. ...... 4 A. General concept of gley mechanisms... 4 B. Matrix color.. ....................... 5 C. Mottles with depth and color......... 7 D. Concretions .......................... 11 Materials and Methods ....... . ....... ....... 14 A. Field Work... ............ ...... ..... . 14 B. Laboratory Analyses......... ......... 17 Results and Discussion... ...... . ..... ...... 18 A. Marlette Series...... ........ . ...... . 18 B. Capac Series... ..... .......... ....... 38 C. Parkhill Series....... ............... 42 D. Brookston Series ....... .... ..... ..... 44 Summary and Conclusions ....... .... ..... .... 45 Appendix A ..... . .............. . ............ 49 Appendix B ........ . ....... . ....... .. ....... 59 References ..... . ...... . ........ . .......... 69 LIST OF TABLES Table Page 1. Moisture contents (Z by volume) of 30, 60, 90, and 120 cm depths at different tensions .................. 22 2. Moisture contents (Z by volume) of 30, 60, 90, and 120 cm depths in three pedons at different tensions.. 24 3. Water table fluctuations (depths in cm) in nine pedons ............................................... 25 4. Some morphological properties of nine pedons ......... 26 5. Temperature (‘E) fluctuations in nine pedons ......... 29 6. Bulk density and hydraulic conductivity of nine 000000000000 00000000 0000000000000 00000 0000 35 pedons..... 7. Soil moisture readings (Z by volume) of pedon M1..... 50 8. Soil moisture readings (Z by volume) of pedon M2 ..... 51 9. Soil moisture readings (Z by volume) of pedon M3 ..... 52 10. Soil moisture readings (Z by volume) of pedon C1.... 53 11. Soil moisture readings (Z by volume) of pedon C2.... 54 12. Soil moisture readings (Z by volume) of pedon C3... 55 13. Soil moisture readings (Z by volume) of pedon Pl.. 56 14. Soil moisture readings (Z by volume) of pedon P2.... 57 15. Soil moisture readings (Z by volume) of pedon BI... 58 Figure 10 10. 11. 12. 13. LIST OF FIGURES Fluctuations of saturated zone in three Marlette pedons based on neutron moisture meter data...... Fluctuations of saturated zone in three pedons of Capac series.... ..... ........ Fluctuations of saturated zone in two Parkhill pedons and one Brookston pedon.... Hydraulic conductivity (cm/hr) in nine pedons of four soil series............. Soil Soil Soil Soil Soil moisture moisture moisture moisture moisture characteristic characteristic characteristic characteristic characteristic curves curves curves CUIVES curves of of of of of Pedon Pedon Pedon Pedon Pedon M1..... M2 ...... M3000 C1000 C2 ...... Soil moisture characteristic curves of Pedon C3.. Soil moisture characteristic curves of Pedon Pl.. Soil moisture characteristic curves of Pedon P2.. Soil moisture characteristic curves of Pedon Bl.. vi Page 19 20 21 37 6O 61 62 63 64 65 66 67 68 INTRODUCTION Natural drainage is defined as the frequency and duration of periods when the soil is free of saturation (USDA, 1951). According to this concept, soil scientists have assigned soils to seven drainage classes, ranging from poorly drained to excessively drained. The downward flow of water through a soil is affected by permeability and location of the water table. Therefore, fluctuations of a seasonal water table have posed particular problems to many soil uses and management, and are often problems whenever near the soil surface. CrOp growth, building, septic tank operation, waste disposal, and off-road traffic may be impaired or limited by periodic high water tables. To assist planners in making land-use decisions, such as evaluation of soil productivity, determination of land area to be drained, and use for both agricultural and nonagricultural purposes, detailed soil information is needed. This information includes evaluation of ground water behavior. The later could be carried out in a satisfactory manner through monitoring of soil moisture regimes for long periods of time, plus detailed soil descriptions and some important physical and chemical properties. Such information would pave the way to find reliable criteria from morphological features to estimate the depth and duration of saturated soil zones. Conspicuous soil features such as soil matrix colors, coating colors, mottles, and concretions are being used in the soil-survey program as evidence of different degrees of wetness. Soil Survey Staff (1975) have in- dicated that mottles occur as a result of fluctuations of groundwater levels and periodic soil saturation. More specifically, mottles with chromas of 2 or less have been used in the USDA Soil Taxonomy System as indicators of significant soil saturation. Alternation of oxidation and reduction is an essential process in the development of gley. This phenomenon is caused by anaerobic conditions or reduction reaction involving the reduction and mobilization of iron. The intensity of reduction in soil saturated with water depends on the activity of microorganisms and the content of decomposible organic matter (Brummer, 1973). Reduction occurs due to the deficiency of oxygen which occurs as a result of rising water table and activ- ities of different microorganisms. Therefore, the reduced iron compounds either would be removed from the soil with downward movement of the water, or would be redistributed within the soil. These oxidation-reduction cycles are commonly characterized by the formation of various colors within the soil profile ranging from gray to reddish-brown colors. In this study, depth and duration of saturated zone were related to soil morphological features. To meet this objective the following secondary objectives were identified: 1. Monitor the depth of saturated zone throughout the year in soils occurring in three representive hydro-sequences in two counties (Clinton and Ionia) in Michigan. 2. Study the relationship between soil morphological features and depth and duration of saturated zone, in an attempt to find reliable criteria for predicting the zone of saturation. 3. Determine saturated hydraulic conductivity in the laboratory and in-situ, bulk density and water contents at 0.0, 0.06, 0.1, 0.33, l, 3, 5, and 15 bar tensions. LITERATURE REVIEW A. General concept of gley mechanisms Gley occurs under saturated conditions as a secondary process following intensive reduction and mobilization of iron (Ottow, 1973). The removal or loss of iron from the profile leaves the soil a neutral gray color with a low chroma, which has been associated with the saturated zone without respect to length of saturation (Soil Survey Staff, 1975). Thermodynamically, the transformation of trivalent iron to divalent iron requires energy. Anaerobic microorganisms are capable of decomposing organic matter and fixing nitrogen to maintain their activity. Organic matter and saturation are essential for the reduction of iron. A proposed mechanism of gley formation is as follows (Ottow, 1973): Inorganic fermentation (Clostridium sp.): energy substrate ‘ a + H+ + ATP + end source dehydrogenases7 products Iron oxide as hydrogen acceptor: - +2 >Fe - on + H+ + e «+% Fe + 2H20 Gley formation: +2 2Fe(OH)3 + Fe + 2011‘-«-;-___-‘- Fe3(0H)8 brown green-gray Anaerobic, nitrogen—fixing clostridia, capable of reducing iron oxides vigorously, are proposed in this mechanism. B. Matrix Color The relationship of groundwater table to certain morphological soil features indicated that a chroma of 2 was related to a long period of saturation in that horizon (Gile, 1958; Fanning et al., 1973; Laing, 1973; McKeague et al., 1973; Veneman and Boding, 1982). A similar study was carried out on four seasonally saturated soils to determine if each soil had an aquic moisture regime (Vepraskas and Wilding, 1983). Despite the sign- ificant periods of saturation and reduction, a chroma of 2 or less was not found in all soils. Rather, a chroma of 3 was found on ped surfaces in some saturated horizons. Therefore, Vepraskas and Wilding (1983) recommended chromas of 3 and less as indicative of an aquic moisture regime. This chroma, 3, has been reported on ped surfaces in Bg horizons of soils included in several studies (Buringh, 1960; McKeague et al., 1969, 1973; Laing, 1973; Vepraskas et al., 1974). The B—horizon of some- what poorly drained soils had a chroma of 3 after kneading (Richardson and Hole, 1979). Values of 4 or 5 with mottles were often associated with a chroma of 3 in all these studies. A chroma of 2 or less have been questioned as a suitable criterion for soils developed on red parent materials or reddish—brown deposits (McKeague and Cann, 1969). Several studies that were conducted on the re- lationship between soil morphology and soil water regimes have indicated that matrix colors with hue of 2.5Y and values of 5 and 6, were found in horizons that were saturated with water for a significant period of time (Gile, 1958; Simonson and Boersma, 1972; Fanning et al., 1973; Laing, 1973; McKeague et al., 1973; and McArthur and Russell, 1978). In several studies, matrix colors with a hue of 5Y and a value of 5 were associated with horizons that were saturated for prolonged periods (Gile, 1958; Simonson and Boersma, 1972; Laing, 1973; McKeague et al., 1973; Veneman and Bodine, 1982). Hues of 5Y and 2-5Y with low chromas and in connection with mottles were applicable criteria for identifying the degree of soil wetness with inference of reducing conditions and removal of iron compounds in the profile (Soil Survey Staff, 1951). The yellow hues were not common in soils that have been derived from red parent materials, in spite of excess soil water and restricted downward movement of ground- water. Hues of SYR and 10YR, in association with mottles, were found in poorly drained soils having red parent materials (Laing, 1973). C. Mottles with Depth and Color Mean highest water table (MHW) and mean lowest water table (MLW) in several soils were determined on the basis of measurements of groundwater levels (Van Wallenburg, 1973). Brown mottles with hues of 5YR-10YR began above the MHW. Distinct brown mottles with hues of 2.5Y-10YR were abundant below the MHW. Therefore, the presence and location of brown mottles at a certain depth did not give a reliable indication of water-table levels. Distinct gray mottles, mostly with hues of 2.5Y to ICC and chromas of l or less, were always found between MHW and MLW. The upper boundary of the horizon with distinct gray mottles was located between 10 and 50 cm below the MHW in different profiles. The position of this layer with respect to the MHW was dependent on texture, parent material and soil structure. The MLW was related to the depth of the G—horizon. Similar results had been reported by Schelling (1960). He noted that gray mottling was always a reliable indicator for estimating mean highest water table, but he didn't indicate the hue or chroma of these mottles. Profile descriptions of soils in representative topo- sequences revealed that mottles with low chromas of 2 or less on ped exteriors and high chromas of 6 or more inside peds occurred in zones that were saturated for short periods of time (Blume, 1968; Veneman and Bodine, 1982; Richardson and Lietzke, 1983). Mottles with low chromas of 1 inside peds and with high chromas of 5 or more on ped exteriors and a lack of manganese coatings or nodules occurred in almost continously saturated zones (Veneman et al., 1976; Richardson and Lietzke, 1983). Horizons that were saturated for short periods of time, and periods of several months near saturation, had mottles with a chroma of 2 inside the peds with few manganese mottles (Veneman et al., 1976). Thus, mottles with low chromas of 2 or less inside peds and high chromas on ped surfaces often occurred in soil horizons that were saturated with water for significant periods of time. Several studies have been conducted on the relation between types of mottling and different soil moisture regimes ranging from well-drained to very poorly drained soils (Veneman et al., 1976; Richardson and Hole, 1979; Richardson and Lietzke, 1983). Their studies showed that mottles with a chroma of 1 inside peds and high chromas of 6 to 8 on ped exteriors were dominant in poorly drained soils; mottles with a chroma of 2 inside peds were correlated with somewhat poorly drained soils; and mottles with chromas of 3 or more inside peds were dominant in moderately well drained soils. Zobeck et al., (1983) related the depth of low chroma mottles, 2 or less, to the depth of water table. They reported that these mottles were observed in the 50-100 cm zone of well drained soils, in the 25-50 cm zone of moderately well drained soils, and in the 0-25 cm zone of poorly drained soils. Light gray to light brownish gray (10YR 7/2- 6/2) mottles commonly occurred at depths that were saturated 50 percent of the time (Daniels et al., 1971). The depths at which faint and distinct mottling occurred were found to be highly correlated with a high degree of soil wetness (Simonson and Boersma, 1972). To illustrate this, certain relationships between the occurrence of both types of mottling and water-table levels are listed below. 10 Avg. percentage of Depths of time the water table Type of soils faint mottles was above the depth Willamette (well 127.0 cm 90.3, 91.0, 88.1, 73.2, drained). 16.2, 0.5 (January through Woodburn (moderately 76.2 cm June, respectively) well drained) Amity (somewhat poorly 33.0 cm drained) Concord (poorly drained) 15.2 cm Dayton (poorly drained) 15.2 cm Depths of Avg. percentage of distinct time the water table Type of soils mottles was above that depth Willamette (well 152.4 cm 93.4, 95.0, 94.0, drained) 86.3, 43.0, 9.1 (January through Woodburn (moderately 114.3 cm June, respectively) well drained) Amity (somewhat poorly 94.0 cm drained) Concord (poorly drained) 15.2 cm Dayton (poorly drained) 15.2 cm Distinct mottles with some grayer—colored mottles with hues of 2.5Y and 5Y occurred in horizons that were saturated for a long period of time. 11 D. Concretions Arshad and Arnaud (1980) studied some soils of Saskatchewan and reported that the presence of concretions was most evident under conditions of restricted drainage. These conditions are suitable for resegregation of Fe, Al, Mn, and organic matter in concretionary forms with B-horizons. The contents of both Fe and P increased with the decreasing size of concretions, whereas the amount of Mn was directly related to the size of concretions. Distribution and development of concretions have been reported under different soil moisture regimes (Simonson and Boersma, 1972; Richardson and Hole, 1979; Arshad and Arnaud, 1980). Concretions were absent in well-drained soils; abundant in somewhat poorly drained soils, and few in poorly drained soils. A recent study showed that there are few concretions in the soil zone which is normally saturated, while plentiful in zones with fluctuating water tables (Richardson and Lietzke, 1983). A study of gray hydromorphic soils of the Hawaiian Islands indicated that all soils, with the exception of those moderately well and well-drained soils, showed a drop in free iron, Fe203, at depths around 50 cm (20 in.) (Russian and Swindale, 1974). This depth coincided with 12 the depth of the water table. The vertical distribution of free MnO2 and Fezo3 decreased with the indreasing hydromorphism (the process that leads to the development of properties caused by poor drainage conditions). Bloomfield (1952) indicated the the gley horizon might contain high free iron due to periodic aeration and oxidation of ferrous iron. Thus, free iron analysis may not be a reliable method in differentiating soils of different moisture regimes. Maclead (1973) reported that the ratio of ammonium acetate extractable Mn to total Mn increased significantly as the groundwater was approached in some soils of eastern England. The ratio of ammonium acetate extractable Fe to total Fe was small compared with Mn. The ratio of iron was between 0.09-0.S and that for Mn of 0.49-2.41. Field studies on the soils southwest of Paris indicated that the thickness of A horizons in poorly drained soils 2 was related to the fluctuation of water-table levels (Fedoroff, 1973). The same study showed that the gray color of the AB horizon was related to the duration of the impedence. McArthur and Russell (1978) noted that the thickness of A2 horizon increased with restricted drainage. Criteria for the classification of Weiesenboden soils of'Iowa, which have been developed under conditions of 13 periodically high water tables were dependent on the thickness of the A horizon and the presence of a strongly mottled, light olive gray gley horizon below the lower B horizon (Riecken, 1945). In southern Ontario and parts of Quebec, the difference in characteristics between A and B horizons became less distinct as drainage 2 2 became poorer (Stobbe, 1952). MATERIALS AND METHODS A. Field Work Three representative hydrosequences were selected and sampled for this study. Hydrosequences 1 and 2 are situated in Clinton County within one-half mile of each other, near the town of Maple Rapids. Both hydrosequences are composed of three series: Marlette, Capac, and Parkhill. The third hydrosequence is situated in Ionia County near the town of P310, and is composed of Marlette, Capac, and Brookston. The soils on the upper slopes (pedons M1, M2, and M3) are representative of the Marlette series, which is classified as fine-loamy, mixed, mesic Glossoboric Hapludalf. Pedons M1 and M3 are well-drained soils, while pedon M2 is moderately well drained soil. The soils on the foot slopes (pedons C1, C2, and C3) are the somewhat poorly drained Capac series which is classified as fine-loamy, mixed, mesic Aerie Ochraqualf. Pedons P1 and P2 occur on toe- slope positions and are representative of the Parkhill series, which is poorly drained and is classified as fine— loamy, mixed, mesic Mollie Haplaquept. Pedon BI is representative of the poorly drained Brookston series, which is classified as fine-loamy, mixed, mesic, Typic Argiaquoll. These pedons have been described elsewhere (Cremeens, 1983). 14 15 The parent material of the hydrosequences in both counties is glacial till. The forest vegetation on the well-drained Marlette soil in hydrosequence 1 consists of Shagbark Hickory (Carya ovata), White Oak (Quercus alba), and Northern Red Oak (Quercus rubra); on the somewhat poorly drained Capac soil, consists of Sugar Maple (Acer succharum), White Oak, and Shagbark Hickory; and on the poorly drained Parkhill soil, consists of White Oak, Quaking Aspen (Populas tremuliodes), and Swamp White Oak (Quercus bicolor), (Cremeens, 1983). This poorly drained site also has a dense cover of Yellow Nutsedge (Cyperus esculentus). Hydrosequence 2 is situated in a ISO-acre woodlot consisting of America Basswood (Tilia Americana), Sugar Maple, and Northern Red Oak on the well-drained Marlette soil; Sugar Maple, Northern Red Oak, Red Maple (Acer rubrum), and Shagbark Hickory on the somewhat poorly drained Capac soils; and White Oak, White Ash, (Fraxinus Americana), and Swamp White Oak on the poorly drained Parkhill soil. Yellow Nutsedge occurs on most parts of the poorly drained site. Hydrosequence 3 is situated in a wooded area consisting of Pin Oak (Quercus palustris), White Oak, and Shell Bark Hickory (Carya laciniosa) on the well- drained Marlette soil; Shagbark Hickory, Bitter Nut l6 Hickory (Carya cordiformis), White Oak, and Quaking Aspen on the somewhat poorly drained Capac soil; and Sugar Maple, American Basswood, and Slippery Elm (Ulmus rubra) on the poorly drained Brookston soil. Five undisturbed soil cores were taken from each of four depths (30, 60, 90, 120 cm), at which percent moisture was determined every two weeks using a neutron moisture meter. Neutron moisture meter access tubes with an inside diameter of 51 mm and lengths of 1.5- 3.0 meters were installed at all sites. Access tubes were aluminum tubing with one end sealed with a rubber stopper and silicon sealer. A hole was augered near each of the sampled pedons using a bucket auger with a 63.5 mm diameter bucket. A restrictive layer such as coarse fragments or water prevented angering to 3.0 meters in some of the sites. The aluminum tubes were inserted into the holes and the annular space around the tubes was filled with soil material and sealed tightly to above the soil surface to prevent seepage. Saturated hydraulic conductivity was measured in-situ for three different depths, (50, 100, and 150 cm). The tubes, consisting of aluminum tubing with an inside diameter of 3.6 cm, were installed near each neutron moisture access tube at each site. The 50 cm tubes 17 were not installed at sites M1 and M3. In-situ hydraulic conductivities were measured in the observation wells by pumping water out of the wells and measuring the rates at which the water levels rose in the wells. A Soiltest model Dr 760A water-level indicator is battery operated, and a needle moves once the end of the drop source comes into contact with water. Thermocouples were installed in each of the sampled pedons at depths of 30, 50, 60, and 90 cm. Soil temp- eratures were measured every two weeks using an Omega Digital temperature indicator, model 199. B. Laboratory_Analy§es Bulk density was determined using undisturbed cores (Soil Survey Staff, 1972). Soil moisture contents at 0, 0.06, 0.1, 0.33, and 1 bar tensions were determined using undisturbed soil cores. Disturbed samples were used for determining soil moisture contents at 3, 5, and 15 bar tensions using porous plate apparatus (Soil Survey Staff, 1972). The undisturbed soil cores for three pedons, C2, P2, and B1, were resaturated for estimating their moisture contents at 0, 0.01, 0.02, 0.03, 0.04, 0.05 and 0.06 bar tensions. Results and Discussion Seasonal variations in the depths of the saturated zones in nine forested sites representing four soil series are shown in Figs. 1, 2 and 3. These figures were constructed from neutron moisture meter data (Appendix A), and volumetric water contents at saturation for undisturbed cores (Table 1 and 2). The data obtained with the neutron moisture meter was supported by measurements of water table levels in series of pipes in each site (Table 3). Marlette series The Btl horizon (28-63 cm) of pedon M1 has a brown matrix color with a chroma of 4 and argillans (clay films) with a chroma of 2 (Table 4). The 30 cm depth was satur- ated for 4 weeks and the 60 cm depth was saturated for 6 weeks (Fig. 1). The same colors suggest that there is no significant difference between 4 and 6 weeks soil saturation as far as reduction is concerned. This is probably due to a short period, 1-2 weeks, when the soil temperature (Table 5) was above biological zero (5 L) and the horizon was saturated for both depths. The 30 and 60 cm depths were also near saturation for an additional 2-4 weeks when the soil temperature was above SlT. In 18 Depth (cm) Depth (cm) Depth (cm) 19 Pedon Ml 01 l 1981 f 1982 IIII .. 1983 00000 1984‘ A A b I 1981 000 l’ 19830000 60 . . q ' 1984AAA r 180 I f l l W A1 1 I A Al ‘ Pedon M3 0.. 19810 00 .. 1982 F F 1983 no. 60 a 1984 - - . H "I— 120.. P 180 ,t - - r 1 TI 1 I I V “F "r v 0 10 20 30 40 50 Weeks of Year Fig. 1 - Fluctuations of saturated.zonexin three Marlette pedons based on neutron moisture meter data. Depth (cm) -Depth (cm) Depth (cm) 20 Pedon C1 0‘ f 60‘ 1981 000 ‘ 19 III 120‘, .82 1983’III ‘l 1984000 180 Pedon C2 0‘ q «——0—-4F——0-7x (“Ff 1981000 " 1982I I I 120‘ 19830000 1984AAA d 180 1 1 I I l Pedon C3 0— q 60- .J 1981000 19820 I I 120... 19830000 1984 AAA ‘ J 180 ' ' I v I 1’ 1‘ I'fi‘ 0 10 20 30 Weeks of Year Fig. 2 - Fluctuations of saturated zone in three pedons of Capac series. Depth (cm) Depth (cm) Depth (cm) 21 Pedon P1 O'r 1 81 60- 9 401010 1982I I I ‘ 1983I I I 120‘ 1984AAA 150 ‘_1* r’ r’ I 1’ 1* TI 1’ r r Pedon P2 0" 60- I'll ‘ 19810 00 ' 1982IIII 0 170.1 1983I I I _. 1984000 180 T ‘T* ’T’ 1’ 1 1 r ’1 ? Pedon B1 0‘ qF—£>——4h——.r—4H—.B <0-A40 60" 19810 0 0 '1 1982I I I 1204 1983 000' 1984AAA 180 ‘ I T r T r I T ET I j 0 10 20 30 40 50 Weeks of Year Fig. 3 - Fluctuations of saturated zone in two Parkhill pedons and one Brookston pedon. 22 TABLE 1 MOISTURE CONTENTS (Z BY VOLUME)OF 30, 60, 90 AND 120 CM DEPTHSHNTDIFFERENT TENSIONS Tension (bar) Pedon Depth N°' (cm) 0 0.06 0.1 0.33 1 3 5 15 M1 30 40.4 33.0 31.7 30.5 29.2 16.8 13.7 7.9 60 45.2 38.5 37.4 35.9 34.8 16.8 13.5 7.9 90 39.9 32.9 31.6 30.1 29.1 21.5 18.6 14.9 120 38.7 31.4 30.7 28.3 27.2 16.8 15.3 9.7 M2 30 42.8 33.4 32.9 32.2 31.4 18.5 18.0 14.9 60 41.3 34.7 34.2 33.2 32.7 23.8 20.2 16.7 90 39.2 30.1 29.5 28.4 27.3 18.1 16.7 14.0 120 38.1 29.8 28.9 28.2 27.3 18.5 17.1 14.1 M3 30 39.4 30.8 29.4 27.7 26.9 14.5 12.3 8.8 60 42.7 35.5 34.8 32.8 31.7 15.4 13.7 11.4 90 39.3 32.4 31.3 28.5 27.6 11.5 10.9 6.2 120 37.4 31.4 30.1 28.3 27.5 11.2 10.8 6.1 01 30 43.8 37.1 36.2 35.2 34.8 18.9 14.9 13.2 60 41.3 33.9 33.6 32.7 31.9 20.3 18.0 14.1 90 37.5 30.7 28.9 27.2 25.2 20.0 18.0 14.1 120 34.9 29.2 28.6 27.1 25.0 19.4 16.7 14.4 02 30 41.3 39.5 31.2 27.9 26.4 12.8 9.7 7.9 60 40.0 31.2 39.9 26.2 24.6 12.8 11.0 7.9 90 39.2 30.2 28.6 25.4 23.9 12.7 10.9 7.8 120 39.3 31.9 30.4 27.2 25.5 17.2 15.3 10.5 C3 30 40.4 29.0 26.4 23.9 22.6 13.2 11.5 60 41.1 29.4 27.1 23.2 21.9 12.8 10.5 90 40.1 28.5 25.2 22.5 21.7 12.7 10.5 . 120 34.9 26.6 24.2 21.9 20.6 10.1 9.3 . 23 TABLE 1—-continued Pedon Depth Tension (bar) No. (cm) 0 0.06 0.1 0.33 1 3 5 15 P1 30 59.1 49.6 47.6 47.6 46.9 26.9 22.4 18.4 60 55.7 46.9 46.3 45.3 44.6 27.8 24.6 21.0 90 50.1 44.6 43.9 43.5 43.2 23.4 19.9 15.8 120 40.6 36.6 35.9 34.9 34.4 18.5 15.4 12.3 P2 30 49.9 42.0 40.4 38.4 37.5 18.5 16.3 12.3 60 44.1 36.1 34.3 32.3 30.8 16.3 14.5 11.4 90 39.7 35.5 34.0 31.9 30.5 16.3 14.4 12.3 120 37.7 33.4 31.6 30.3 29.1 16.3 13.9 10.4 B1 30 48.4 35.1 32.1 29.8 28.5 10.6 9.2 7. 60 46.7 36.2 35.2 30.8 29.6 11.0 10.2 7. 90 46.5 37.8 35.2 32.5 31.3 10.6 8.3 7. 120 46.9 40.7 38.7 36.4 35.0 10.6 8.3 7. 24 TABLE 2 MOISTURE CONTENTS (Z BY VOLUME) OF 30, 60, 90 AND 120 CM DEPTHSIN THREE PEDONS AT DIFFERENT TENSIONS Tension (bar) Pedon Depth No. (cm) 0 0.01 0.02 0.03 0.04 0.05 0.06 oz 30 39.3 36.2 35.4 34.8 34.1 33.4 32.8 60 38.3 35.4 34.7 34.0 33.3 32.6 31.7 90 37.5 34.3 33.2 32.9 32.0 31.3 30.5 120 38.0 35.2 34.5 34.0 33.3 32.6 32.0 P2 30 51.8 45.1 44.0 43.3 42.6 42.0 41.7 60 42.5 39.2 38.3 37.7 37.0 36.3 35.7 90 39.1 36.7 36.2 35.9 35.4 35.0 34.7 120 38.0 35.1 34.3 33.8 32.8 31.7 29.3 B1 30 49.8 41.3 39.5 37.9 36.7 35.7 35.1 60 46.8 41.6 40.1 38.8 37.7 36.6 35.9 90 46.2 42.3 41.2 40.1 38.9 37.8 37.0 120 46.2 43.4 42.6 41.8 41.0 40.2 39.9 TABLE 3 WATER TABLE FLUCTUATIONS (DEPTHS IN CM) IN NINE PEDONS 1983 1984 pN* WD** N J M M1 100 - - - - - - 53 67 16 29 27 60 69 40 150 - - 150 - 150 150 28 67 16 26 27 60 69 <- M2 50 - — - - - - - - 4O 45 37 - 49 - 100 - - - - - 63 75 47 51 47 59 60 64 150 - - 140 150 150 66 76 45 51 47 59 60 64 M3 100 - 90 90 - - - - - — — — — — — 150-—-—----——-___ C1 50 - - 4O - — - 43 45 14 19 13 21 24 27 100 - - 46 - - - 40 44 17 24 16 27 27 28 150 - 150 41 140 148 150 41 43 14 20 16 28 28 28 C2 50 - - 50 43 47 - 16 39 10 5 7 16 23 27 100 - - 59 49 48 64 14 39 16 12 13 17 25 29 150 - 150 109 93 64 63 56 38 47 32 28 20 32 39 C3 50 — - -' .33 32 40 13 30 - 5 4 16 23 15 100 - - 67 33 34 41 14 33 60 10 12 19 25 19 150 150 150 67 30 37 43 13 34 60 10 9 17 26 18 P1 50 — - 32 26 29 25 20 10 4 — - 3 100 - - 31 27 28 23 21 11 5 - - 6 150 148 109 30 29 27 21 23 12 4 - - P2 50 - 28 20 32 4O 46 23 27 20 10 - 13 20 13 100 - 30 23 3O 4O 47 24 23 20 12 13 10 23 15 150 150 33 21 33 4O 43 20 25 20 14 10 13 21 19 BI 50 - - 15 24 27 9 13 20 - - 10 14 9 100 - - 12 24 25 12 14 2O 3 12 13 12 150 - 120 11 24 23 11 14 21 3 4 11 15 10 *Pedon Number. **W611 Depth (cm). 26 TABLE 4 SOME MORPHOLOGICAL PROPERTIES OF NINE PEDONS* (FROM CREMEENS,1983) Color Horizon fifififi; Texture 3:32:- Matrix Mottles Coatings Pedon M1 A 0-10 SiL 2fgr 10YR 4/2 E 10-19 SiL 1fpl 10YR 6/3 BE 19-28 L 2msbk 10YR 5/4 Btl 28—64 L 2msbk 10YR 4/4 10YR 4/2 Bt2 64—97 CL 2msbk 10YR 4/3 10YR 4/2 BC 97-104 SiL 2csbk 10YR 4/3 flf 10YR 4/4 10Y 3/2 Cl 104-165 SiL lcpl 10YR 5/3 flf 10YR 5/6 02 165+ SiL lcpl 10YR 4/3 m3f 10YR 5/6 Pedon M2 A 0-12 SiL 2mgr 10YR 4/2 E/B 12—26 SiL lmpl 10YR5/6 2msbk 10YR 6/6 Btl 26-40 SiCL 2msbk 10YR 4/4 10YR 4/2 Bt2 40-84 SiCL 2mabk 10YR 4/4 flf 10YR 5/4 10YR 4/2 BC 84-108 SiL 3cpl 10YR 4/4 f2f 10YR 5/4 10YR 4/2 2msbk Cl 108—165 SiL 3cp1 10YR 5/2 f2f 10YR 5/4 2msbk C2 165+ SiL 3cpl 10YR 5/3 clf 10YR 5/4 Pedon M3 A 0-12 L 2mgr 10YR 4/2 B/E 12-32 L lmpl 7.5YR474 2fsbk 10YR 5/2 Btl 32-48 L 3fsbk 7.5YR 4/6 10YR 4/3 Bt2 48-86 L 2msbk 7.5YR 5/4 7.5YR 4/2 BC 86—127 SiL 3mpl 10YR 5/3 7.5YR 3/4 2mabk C 127+ L 3cpl 10YR 4/3 fld 5YR 5/6 2cabk 27 TABLE 4--continued D 8 Color Horizon epth Texture truc— (cm) ture Matrix Mottles Coatings Pedon C1 A 0—12 L 2fgr 10YR 3/2 BA 12-25 L 2msbk 2.5Y 6/2 m2p 7.5YR 5/6 Btgl 25-40 L 2msbk 5Y 6/2 m3p 7.5YR 5/8 Btg2 40-110 CL 2msbk 5Y 5/1 c3d10YR 4/6 10YR 4/2 C 110+ SL 2mbk 10YR 5/3 Pedon C2 A 0—22 L 2mgr 10YR 3/1 B/E 22-32 SL lfsbk 10YR 5/3 flf 7.5YR 5/6 10YR 6/4 Bt 32-53 L 2mabk 10YR 5/3 C2d 7.5YR 4/4 7.5YR 4/2 & f2f 10YR 5/2 Btg 53-97 L 2msbk 2.5Y 4/2 c2d 7.5YR 4/4 10YR 5/2 & f2d 10YR 5/3 BC 97—125 SL 1msbk 2.5Y 4/2 m2p 7.5YR 5/6 10YR 5/2 & cld N 5/0 2C 125+ SiL 2cpl 2.5Y 4/4 c3d N 5/0 1cabk & mld 10YR476 Pedon C3 A 0-17 SL 2fgr 10YR 3/1 B/E 17-33 L 2fsbk 10YR 4/4 10YR 4/2 10YR 5/3 Bt 33-58 L 2fsbk 10YR 4/4 cld 2.5Y 5/2 & c2d 7.5YR 4/6 10YR 4/3 Btg 58-85 L 2msbk 2.5Y 5/2 C2d 10YR 4/4 & cld 10YR 5/2 10YR 4/2 BC 85-160 SL 2cp1 10YR 5/6 mld 10YR 6/1 SYR 5/4 2pr & c2d SYR 5/4 C 160+ L 10YR 6/3 m2f 10YR 6/1 & f3d 7.5YR 4/4 28 TABLE 4--continued Color Horizon aigsr Texture i:;::_ Matrix Mottles Coatings Pedon P1 A 0-16 SiL 2mgr 10YR 3/1 BA 16-25 SiCL 2fsbk 2.5Y 4/2 f2d IDLYR 5/1 & fld 7.5YR 5/6 Bgl 25—46 SiCL 3mabk 5Y 4/1 c2p 7.5YR 4/6 2fsbk & cld 10YR 4/4 Bg2 46-85 SiCL 3mabk 3fsbk N 5/0 m3p 7.5YR 4/6 cld 10YR 4/4 Bg3 85—119 SiCL 2mabk N 5/0 m2d10YR 4/4 2fsbk & 10YR 4/6 C 119+ SiL 2mabk 10YR 5/3 m3d NS/O & c2d 7.5YR 4/4 Pedon P2 A 0—23 SiL 3vfsbk 10YR 3/2 Bgl 23-53 L 2fsbk 5Y 4/1 fld 10YR 4/3 flp 5YR 4/6 Bg2 53-91 L 2msbk 5Y 5/1 c1p 7.5YR 5/6 2fsbk C 91+ L m 2.5Y 4/2 c2010YR5/3 N6/0 & 7.5YR 5/6 Pedon B1 A 0-25 SL 2mgr 10YR 2/1 BA 25-40 SL 2fsbk SY 4/1 f1d10YR 4/2 8th 40-58 L 1msbk SY 5/2 C2d 10YR 5/4 SY 5/1 2fsbk Btg2 58-95 L lcpr 5Y 5/1 f1d10YR 4/4 N 5/0 2msbk BC 95—170 SL lfsbk 5Y 5/1 mlp 7 .SY 5/6 5Y 5/2 C 170+ L m 10YR 4/4 c2d N 5/0 *Abbreviations according to Soil Survey Staff, 1951. 29 TABLE 5 TEMPERATURE (°C) FLUCTUATIONS IN NINE PEDONS 1984 1983 Depth (cm) Pedon No. 7 7 7 7 6 6 6 6 7 7 7 7 6 7 7 6 6 6 6 6 7 7 7 8 7 7 7 6 6 6 6 5 7 6 6 6 7 7 6 6 7 6 6 6 8 7 6 6 8 7 7 5 8 6 6 5 7 6 6 5 8 7 6 4 8 7 6 4 8 7 7 4 6 5 5 4 5 4 4 4 5 5 5 4 6 5 5 S 5 5 5 4 6 6 6 5 2 2 2 3 2 2 2 3 2 2 2 3 2 2 2 3 2 2 2 3 2 2 2 3 1 2 2 3 1 2 2 3 1 2 2 3 1 2 2 3 1 1 2 3 1 2 2 3 1 2 2 3 1 2 2 3 1 2 2 3 1 2 2 3 1 1 2 3 . 1 2 2 3 1 1 2 3 1 2 2 3 1 2 2 3 1 1 2 3 1 1 2 3 1 2 2 3 1.. 2 2 3 1 2 2 3 1 2 3 4 1 1 2 3 1 1 2 3 1 1 2 3 0 0 0 2 2 3 4 2 2 3 4 3 3 4 5 2 3 3 4 1 2 2 3 1 2 2 3 3 3 4 5 2 3 4 5 2 3 4 5 3 3 4 5 2 2 3 4 1 2 2 3 3 4 4 5 3 4 5 5 3 4 4 5 3 4 4 5 3 4 4 5 2 4 4 S 5 6 6 7 6 6 6 7 6 6 6 7 6 6 6 7 5 6 6 7 6 5 5 6 6 7 7 7 7 8 8 9 7 7 8 9 7 8 8 9 7 7 8 9 6 7 7 8 9 9 9 0 9 0 O 0 9 O 0 0 9 9 O 0 9 O 0 0 9 0 0 0 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 2 3 3 1 2 2 3 1 2 2 3 1 2 2 3 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 O 1 1 2 1 2 2 2 1 1 2 2 1 1 2 2 1 2 2 2 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 6 7 7 6 6 6 6 5 5 6 6 5 6 6 6 5 6 6 6 5 6 6 6 5 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 8 7 7 5 7 6 6 4 8 8 7 6 7 6 6 4 7 6 6 5 8 7 6 5 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 7 6 6 5 6 5 5 4 6 5 5 4 5 5 5 4 6 6 6 5 5 5 4 3 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 0 0 0 O 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 O O 3 5 6 9 3 5 6 9 3 w ’00 00; 3 5 6 9 3 5 6 9 3 5 6 9 1 2 3 1 2 3 M M . M C C C 30 TABLE 5--continued 1984 1983 Depth (cm) Pedon No. 7776 7777 7778 7776 8776 8776 8664 9876 9876 6555 6555 6655 2334 2233 2233 2334 1223 1223 2334 1223 1223 2334 1223 1223 2334 1223 1123 2445 1123 1123 3456 2234 1123 3456 2557 3445 6778 5566 6667 7789 6778 7789 0001 0001 9000 1111 1111 111 2333 1223 1111 1111 2223 1223 1222 1111 1111 1111 6665 6665 6665 1111 1111 1111 7664 7765 8765 1111 1111 1111 6553 7665 6554 1111 1111 1111 0000 0000 0000 3569 3569 3569 1 2 1 P. P. B 31 this study, near saturation is defined as water held between 0.00-0.005 bar tension. The water contents (% by volume) at this range of tension were obtained from soil moisture characteristic curve of each depth (Appendix B). Argillans with a chroma of 2 are also found in the Bt2 horizon (64-97 cm), but the matrix color has a chroma of 3 rather than 4. The change in the matrix color may be related to a longer period, 12-14 weeks, of saturation in the 90 cm depth and 4-6 weeks when the soil temp- erature was above 5 %. The 90 cm depth had soil moisture tension values near saturation for 2-4 weeks, however, the soil temperature was below 5°C during this time. Faint mottles with chromas of 6 were found in the C horizon (104-165 cm). The 120 cm depth was saturated for 12-14 weeks but the soil temperature was above 5°C for only 4-6 weeks. This depth was near saturation for 2-4 weeks but the soil temperature was below biological zero. Using the morphological features given in Soil Taxonomy, (Soil Survey Staff, 1975), the predicted saturated zone should be at 97 cm where mottles occur. However, saturation occurs as high as 30 cm in this pedon. In some other parts of the United States, well 32 drained soils have high water tables; for example, the well drained Williamette soil in Oregon had a water table at 50 cm depth for a few months each year, and the matrix had a chroma of 3 rather than 2 or less (Simonson and Boersma, 1972). In Indiana, the well drained Zanesville soil had a water table at 0.5 cm depth for 13 percent of the year and the matrix had chromas of greater than 2 (Franzmeier et al., 1983). A well drained soil in Ohio had water tables within 50 cm of the soil surface for at least 3 months in the spring (Zobeck and Ritchie, 1984). Pedon M3 differed considerably from pedon M1 in the fluctuations of the saturated zone throughout the study (Fig. 1). The Btl (32-48 cm) and the Bt2 (48-86 cm) horizons were never saturated during any time of the year. Neither horizon has mottles. The Btl has matrix color of 7.5YR 4/6 and argillans with a color of 10YR 4/3. The Bt2 horizon has a 7.5YR 5/4 matrix color and 7.5YR 4/2 argillans. The color of the argillans (chroma of 2) suggests reduction of iron compounds may have occurred, but the horizon was not saturated. However, the horizon was near saturation for 2-4 weeks during 1983. The soil temperature was greater than 5‘% for 1-2 weeks during this time. Because of mechanical problems with the meter no 33 data are available for spring 1982 or spring 1984. The chromas of matrix and argillans in the Btl horizon of pedon M1 and Bt2 horizon of pedon M3 are identical. The length of time the Btl of M1 was saturated and above 5 % and the Bt2 of M3 was near saturation and above 5°C is similar, 1 to 2 weeks. This could be the reason for the similarity of morphological features in horizons. Apparently, reduction of iron compounds is possible in soils that have their moisture tension approaching zero at the time the soil temperature is above bio- logical zero. Pickering and Veneman (1984) found gray streaking patterns of fragipans in unsaturated soil horizons and related it to reduction which occurred during wet conditions, but not saturations, when soil temperatures were above 5 OC. The BC horizon (86-127 cm) has a matrix chroma of 3 and argillans with a chroma of 4. A perched water table was observed for short periods, less than 3 weeks, at 90 cm. The low hydraulic conductivity in the 90 cm depth (Table 6 and Fig. 4) probably slowed down the water movement and caused a perched water table. This depth was also near saturation for an additional 14-16 weeks but the soil temperature was above 3 % for only 4-6 weeks. Chromas of 3 were observed on ped surfaces 34 of soils that were saturated and had reducing conditions for up to 3 months (Vepraskas and Wilding, 1983). This implies that a chroma of 2 or less is not the only criteria for reduction of iron compounds. Apparently near saturation conditions have a significant effect on the soil mor- phology. A The Btl horizon (26—40 cm) of pedon M2, moderately well drained, has a similar matrix chroma, 4, and argillans color value and chroma of 4/2, as the Btl horizon of pedon M1 and the Bt2 horizon of pedon M3. The Btl horizon of pedon M2 was not saturated, but it was near saturation for 4-6 weeks. The soil temperature was above 5°C for 1-2 weeks, similar to that of the Bt2 horizon of pedon M3. The Bt2 and BC horizon (40-108 cm) have identical matrix, mottles and argillans colors. The matrix and argillans colors are similar to those of the Btl horizon. Thqutl is free of mottles, but the Bt2 and BC horizons have few, faint 10YR 5/4 mottles. The 60 cm depth was saturated for 12-14 weeks and the 90 cm depth was saturated for 14-16 weeks. The soil temperatures were greater than 5 % during only 4-6 weeks. The two depths were near saturation for an additional 2-4 weeks when the soil 0 temperatures were above 5 C. 35 TABLE 6 BULK DENSITY AND HYDRAULIC CONDUCTIVITY 0F NINE PEDONS Laboratory (core method) Piflfn Da£:; Depth 1%;igtu ° B.D.* H.C.** (mean) ° ° gm/cm cm/hr cm/hr M1 30 1.69 3.15 100 3.75 60 1.64 0.42 150 0.88 90 1.79 0.41 120 1.79 0.71 M2 30 1.53 2.44 50 3.50 60 1.60 4.22 100 4.13 90 1.63 2.80 150 1.00 120 1.64 1.43 M3 30 1.72 0.45 100 no water 60 1.62 0.72 150 no water 90 1.69 0.69 120 1.76 0.30 C1 30 1.62 2.11 50 2.65 60 1.67 0.90 100 2.65 90 1.72 0.30 150 0.80 120 1.79 0.33 CZ 30 1.66 0.50 50 1.90 60 1.71 0.23 100 1.00 90 1.70 0.13 150 1.20 120 1.70 0.13 C3 30 1.65 0.98 50 2.70 60 1.66 1.76 100 3.00 90 1.67 1.09 150 1.50 120 1.86 0.55 36 TABLE 6--continued Laboratory (core method) Pedon Depth In-Situ No. (cm) B.D.* H.C.** (mean) H'C' gm/cm3 cm/hr cm/hr P1 30 1.51 9.50 50 -- 60 1.57 4.50 100 8.00 90 1.58 2.83 150 -- 120 1.83 1.52 P2 30 1.43 2.00 50 3.80 60 1.60 0.42 100 0.45 90 1.69 0.30 150 0.37 120 1.71 0.29 BI 30 1.51 7.30 50 8.75 60 1.57 3.50 100 2.95 90 1.59 1.35 150 1.60 120 1.57 0.30 *B.D. = Bulk Density **H.C. = Hydraulic Conductivity, mean of hydraulic conduc- tivity for cores without roots, holes, etc. 37 30.: 143 M2 60... "1 E 8 ,3 90- u O. 0) C3 120- ‘ l I I I 0 2 4 30 60 ’e‘ U V c3 'fi 90 D. 0 G 120 V I I I TI 0 2 4 30" P2 Bl P1 60""I 1:? 3 .c' 90m1 u D. Q) Q 120- l I I f I I r fir u fin 0 2 4 6 8 10 Hydraulic Conductivity (cm/hr) Fig. (4) Hydraulic conductivity (cm/hr) in nine pedons of four soil series. 38 The C1 horizon (108-165 cm) has a matrix chroma of 2 and 10YR 5/4 mottles. It was saturated for 22-24 weeks but soil temperature was above S‘C for only 8—10 weeks. This horizon was near saturation for 4-6 weeks but the soil temperature was above 5 % for 1-2 weeks. Capac Series The results for three pedons (Fig. 2) show that the saturated zones had similar patterns of fluctuations throughout the study. In pedon C1, the Btgl horizon (25—40 cm) has a matrix with a chroma of 2 and prominent mottles with a chroma of 8. The 30 cm depth was saturated for 16—18 weeks but the soil temperature was above 5 T for only 8-10 weeks. 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M5 _ _ 14- . . m.. 0.,H U.. ... . . ., .7 m H ..— "M; :- n . _ _ a m - . , . : 32:05 a v “.3. .....mfim a. wow .8583 99.83....an 956m om v39. 5. ...... -z .. - —" -t "' -s 61 WATER commune; BY VOLUME ) . h . _ ...._ 1 n ....,. . 1"" T: man u. -——_—_. '- H~“-—‘ ' ‘-——-——t - -- —: ..mzzozAmas- . mo». 3..-mafia ngnmonmflwmnwn 05.48 cm v89. 5. .2. .... 62 WATER CONTENT(% BY VOLUME ) ~§¢—t_ ..__._.-..._... . ,. . .7717." f..‘ ,_- ‘. ...- . 5| _ N .. .__, _ -_ . . A 1 ‘ :m __ _“ _ M“. 7 ,,_ -.‘.—H—_—-~- ._.... . , - - . s .. v... . . . mg m. mot apnea... 93.881.an 05.48 cm v39. 9. 63 ‘6 amfi‘m 'ZD uopad go 99m snap-anew 9313810!!! ITOS WATER CONTENT(% BY VOLUME ) __ . 8 “: .§. r‘ “i;i_:f“:f..._-.__-i____-.8..__.::' F g __ f_‘*iif§::;fii;1::f;_:::::T'::_-- ' 1F“:—fl:i__:- :. ' ""' fil‘“::f:‘*f“‘"*—T __-___.___- “ L‘ .7 -Q ‘. " ‘ ‘ - _ .1 ‘ . . . A .. ..__ _ _ ‘-'_’_ .- : ., __-_ . "_ "f1; __ __§_"j' '_- w*--»--- -~-———.—_---—.-<____.._...._ » 7 ‘ ;: ....” »- 1 ‘. w. , _.... ., - I .._'_'I:;:I__'_'_.‘ I” '“—'_ "‘— ~—‘"_" 1“"—°I—:~;: "'—" V 7 . _ r -. .. .-. -. ...... - “2-. _.__.__ __ 23;?:L‘.‘.‘.X._‘L.‘,"TL”-i ' V H. . .. . . I.“ " ' I' M '— ‘ . ‘_ . . .-.. 7- . “ i. - -T‘-: ’ I 7‘ I . . .——t~—--———- —-- - - I ' . O ——.__. ._ ...- . -... . --.. -»»—— — -_-—_ l 1900.0 I I bit 3 I ; I pl; ! 5 I it: I .' j 06- —_ m.--- —.-— f l l u H F n l V ! (Jéqmouual, ; . _ . i .- .! l I l \ 130.3 1: .- I! ! 64 WATER CONTENT(% BY VOLUME ) _ a flaw-...?- _ ...-2:2. .. 22:02.2... awn—um Ho. mob. Bowman... agnmnnmnmmnwn 9.56. cm .599. 0.. 65 WATER CONTENT(% BY VOLUME ) I I _ _.. fig:— ‘ : "-“i‘*‘i*t“fi‘".%f"f‘i‘+f‘/ ‘1 A h . 0 —— ... ’ ‘ O n — —: ---- - _ V l 66 WATER CONTENT(% BY VOLUME ) N v , r, . . m . . . L..htlTLu...-.......Mi . . I6! . . .. — —_—— m. m. 9 m... ‘06.. 8 t — — —:— — r —.1 _¢. 9.1.36... ._ _ ... . 77.”; <8... M ow...- :3 22:02.3; J award 5. mo... Bowman-m 988083...an 9.2mm om 689. w». 67 WATER CONTENT(% BY VOLUME ) -—— “--- “..m_. _ _ _ -, - H L .0 _ _m m : : . m . M. ‘ _ u .- 8.....0- . m ._. .3 . m T- .i- , w _: H i w _ . . m _ L. . _ ._ ‘ ‘8 80.1. T..r........». ... s ’ ‘ _”_:£-_ .2: W0.000“:_: ...-...“. "M; :“ 32:02:.an manna 5. mo? Bonanza... €883.an 93.6. cm 008: E. 68 REFERENCES Arshad, M. A., and R. J. St. Arnaud. 1980. Occurrence and characteristics of ferromanganiferous con- cretions in some Saskatchewan soil. Can. J. Soil Sci. 60:685-695. Bloomfield, C. 1952. The distribution of iron and aluminum oxides in Gley soils. J. Soil Sci. 3: 167-171. Blume, H. P. 1968. Die pedogenetische deutung einer Catena durch die untersuchung der Bodendynamik. Int. Cong. Soil Sci. Trans 9th (Adelaide, Austr.) 4:441-449. Brummer, G. 1973. Redoxreaktionen als merkmalsprangende Prozesse hydromorpher Boden. Pseudogley and Gley: Transaction of Commissions V and VI of the Int. Soc. Soil Sci., pp. 17—27. Buringh, P. 1960. Soils and Soils Conditions in Iraq. Baghdad, Iraq: Ministry of Agriculture. Cremeens, D. L. 1983. Argillic horizon formation in the soils of a hydrosequence. M.S. thesis. Michigan State University. Daniels, R. B., E. E. Gamble, and L. A. Nelson. 1971. Relations between soil morphology and water- table levels on a dissected North Carolina coastal plain surface. Soil Sci. Soc. Am. Proc. 35:781-784. Fanning, D. S., R. L. Hall, and J. E. Foss. 1973. Soil morphology, water table, and iron relation- ships in soils of the Sassafras drainage Catena in Maryland. Pseudogley and Gley: Transactions of Commissions V and VI of the Int. Soc. Soil Sci., pp. 71-79. 7O Fedorof, N. 1973. Interactions de l'Hydromorphie et du Lessivage example d'une Sequence de 8015 Lessives a hydramorphie Croissante Sur limons Quaternaires du Sud-Ouest du bassin de Paris. Pseudogley and Gley: Transactions of Commissions V and VI of the Int. Soc. Soil Sci., pp. 295-305. Franzmeier, D. P., J. E. Yahner, C. C. 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Soil morphological prOperties in relation to depth of the groundwater table in a sandy landscape near Perth, Australia. J. Soil Res. 16:347-349. McKeaugue, J. A., J. H. Day, and J. S, Clayton. 1973. Properties and development of hydromorphic mineral soils in various regions of Canada. Pseudogley and Gley: Transactions of Commissions V and VI of the Int. Soc. Soil Sci., pp. 207-218. McKeague, J. A., J. I. MacDougall, K. K. Laingmaid, and G. A. Bourbeau. 1969. Macro and micro-morphology of ten reddish brown soils from the Atlantic provinces. Can. J. Soil Sci. 49:53-63. 71 McKeague, J. A., and D. B. Cann. 1969. Chemical and physical properties of some soils derived from reddish brown materials in the Atlantic prov- inces. Can. J. Soil Sci. 49:65-78. Ottow, J. C. G. 1973. Bacterial mechanisms of iron reduction and gley formations. Pseudogley and Gley: Transactions of Commissions V and VI of the Int. Soc. Soil Sci., pp. 29-36. Pickering, E. W., and P. L. M. Veneman. 1984. 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Proc. 36: 649-653. Soil Survey Staff. 1975. Soil taxonomy: A basic system of soil classification for making and interpreting soil surveys. Agric Handb. No. 436, USDA. U.S. Government Printing Office, Washington, D. C. 72 Soil Survey Staff. 1951. Soil survey manual. Agric. Handb. No. 18, USDA. U. S. Government Printing Office, Washington, D. C. Soil Survey Staff. 1972. Soil survey laboratory methods and procedures for collecting soil samples. Report No. I., USDA, U. S. Government Printing Office, Washington, D. C. Stobbe, P. C. 1952. The morphology and genesis of the gray-brown podzolic and related soils of Eastern Canada. Soil Sci. Soc. Am. Proc. 16:81-84. Van Wallenburg, C. 1973. Hydromorphic soil charac- teristics in alluvial soils in connection with soil drainage. Pseudogley and Gley: Transac- tions of Commissions V and VI of the Int. Soc. Soil Sci., PP. 393-403. Veneman, P. L. M., and S. M. Bodine. 1982. Chemical and morphological soil characteristics in a New England drainage toposequence. Soil Sci. Soc. Am. J. 46:359-363. Veneman, P. L. M., M. J. Vepraskas, and J. Bouma. 1976. The physical significance of soil mottling in a Wisconsin t0posequence. Geoderma 15:103-118. Vepraskas, M. J., and L. P. Wilding. 1983. Aquic moisture regimes in soils with and without low chroma colors. Soil Sci. Soc. Am. J. 47:280— 285. Vepraskas, M. J., F. G. Baker, and J. Bouma. 1974. Soil mottling and drainage in a Mollic Hapludalf as related to suitability for septic tank con- struction. Soil Sci. Soc. Am. Proc. 38:497-501. Zobeck, T. M., and A. Richie, Jr. 1984. Analysis of long- term water table depth records from a hydro- sequence of soils in central Ohio. Soil Sci. Soc. Am. J. 48:119-125.