单一电解质体系下恒电荷土壤胶体扩散双电层中滑动层厚度的计算

土壤胶体颗粒表面滑动层厚度是一个重要的物理参数。利用Gouy-Chapman理论推导得到单一电解质体系中滑动层厚度计算公式,测得三种紫色土胶体颗粒表面电位值和ζ电位值,通过计算得到滑动层厚度值。结果表明:(1)在2∶1型电解质体系中三种紫色土胶体表面电位和zeta电位绝对值均远低于1∶1型电解质体系,两种单一电解质体系下三种紫色土表面电位值随电解质浓度变化差异要远大于zeta电位值;(2)两种单一电解质体系下三种紫色土胶体滑动层均离双电层中Stern层较远,而与Gouy层靠近,并且在2∶1电解质体系中的滑动层厚度要远低于1∶1电解质体系;(3)三种紫色土胶体颗粒随着电解质浓度升高,其滑动厚度均变薄。不同表面电位土壤胶体颗粒,在电解质浓度较低时,它们的滑动层厚度差异显著;当电解质浓度较高时,它们的滑动层厚度之间差异不明显。     

我国主要变性土的微形态研究

本文研究了变性土三大土类黑粘土、浊粘土,艳粘土的微形态特征。通过大形态、微形态、超微形态观察和膨胀收缩试验揭示了变性土的孔隙、结构、粘粒的就地重新排列以及土壤垒结与土壤粘粒含量、粘粒种类以及土壤膨胀势之间的关系,其中福建浊粘土的微形态特征发育最明显。     

土壤透气性及粘土颗粒比表面积与粘土颗粒粒度分布分形维数关系

采用数字显微系统测定了部分华南地区土壤中粘土颗粒粒径分布分形维数值,提出了土壤中粘土颗粒群粒度分布分形维数的几何法计算模型,并就这种分形维数与土壤比表面积和土壤透气性等性质的相互关系作了初步探讨。结果表明,采用数字显微系统测定的粘土颗粒粒径分布分形维数值介于2.2708到2.9483之间,与常规方法测定结果吻合;含砂较多的土壤样品,BET比表面积和Blaine透气时间随粒度分布分形维数值增大而减小;含粘粒较多的土壤样品,BET比表面积和Blaine透气时间同随粒度分布分形维数值增大而增大。     

碱金属离子在蒙脱石-Cu2+表面吸附的离子特异性

研究离子交换中的离子特异性效应有助于揭示离子-带电表面相互作用机制。以蒙脱石Cu2+饱和样为研究对象,采用恒流法研究不同浓度碱金属离子Li+、Na+和K+的吸附动力学过程,并建立1︰1型(LiNO3、NaNO3、KNO3)电解质溶液中离子平衡吸附量与体系吸附活化能之间的关系。结果发现:(1)Li+、Na+和K+在蒙脱石-Cu2+表面的吸附过程仅呈现出弱静电力作用下的一级动力学特征,并存在明显的离子特异性效应。(2)离子非经典极化作用与体积效应共同决定了离子在双电层中的位置,从而导致表面电位存在差异;并且表面电位(绝对值)随着电解质浓度降低而增加,表现为Li+>Na+>K+。(3)根据新建立的模型可预测吸附离子在双电层中的位置,进而求出体系的吸附活化能,并发现离子特异性效应产生的根本原因是由活化能决定的,同时本研究表明建立的新模型在固/液界面反应中具有普适性。本研究将对固/液界面反应理论的完善提供新思路。     

表面电荷性质对紫色土粘粒悬浮液稳定性影响研究

表面电荷性质对于水体中粘性泥沙颗粒的稳定和聚沉起重要作用，因此本试验测定3种紫色土胶体的表面电荷性质，并讨论其随环境条件改变而变化对紫色土粘粒悬浮液稳定性的影响。结果表明：（1）3种紫色土胶体在2：1型电解质中的表面电位分别约-0．14～-0．192 V．1：1型电解质中约为其2倍，在2种离子体系中的絮凝值分别为0．72～1．12mol／m^3和11．7～17．8mol／m^3，胶体稳定性随其表面电位增加而增强；（2）1：1型电解质中粘粒悬浮液完全沉降时间分别达到40．6～47．0h，比在2：1型电解质中长12．4～14．6h，电解质浓度增加，粘粒悬浮液完全沉降时间下降．稳定性减弱。pH对完全沉降时间影响强烈，当pH=5时，2种电解质体系中的粘粒悬浮液完全沉降时间减少近1／2；pH=3时，60min左右悬浮液已经沉降完全。3种紫色土悬浮液稳定性是酸性紫色土〈中性紫色土〈石灰性紫色土。     

福建主要土壤的粘粒云母含量和供钾潜力

利用X射线衍射法估算了福建省221个土壤样品中粘粒云母含量并讨论了与粘粒云母含量变化有关的因素。结果表明母质是影响粘粒云母含量的主要因素。海积物、河积物及页岩上发育的土壤粘粒云母含量一般较高;基性岩上发育的土壤粘粒云母含量一般较低。风化度较高的赤红壤、红壤、黄红壤和黄壤等土类的粘粒云母含量一般较低。风化度较低的C层的粘粒云母含量一般较B层和A层高,但异源母质的堆积可以使A层粘粒云母含量高于B层和C层。     

耕层土壤颗粒表面的分形维数及其与主要土壤特性的关系

四川 1 6个耕地表层的土壤颗粒表面分形维数D为 2 80 5～ 2 942 ,其中砂土2 82 1、壤土 2 870、粘壤土 2 91 6和粘土 2 939。统计分析表明D分别与国际制粗砂粒和细砂粒含量呈极显著负相关 ,与粉粒和粘粒含量呈极显著正相关 ;它与粉粒、粘粒和有机质含量的偏相关关系达极显著水平 ,与容重的偏相关关系达显著水平     

粘土夹层土体构型水盐运动的实验研究

发育在冲积平原上的土壤,土体中夹有粘土层是很普通的现象。1987年在滨海平原110个土壤剖面调查中,发现粘土层以不同厚度和层位存在时,土壤表现出不同的盐渍状况,该地区粘土层表居很普遍。我们曾对粘土层在浅、中、深三个层位的5、15、30厘米三个厚度对水盐运动的影响作过研究,结果是枯土层对水盐运动的抑制作用随粘土层厚度 钓增加、层位的升高而加强^[2-5]。但是实际调查使我们感到有必要进一步研究土体中粘土层对水盐运动的影响规律,通过毛管水的上行运动的研究,了解粘土层的作用实质。     

用电导热散法研究可变电荷土壤粘粒与离子的相互作用

本工作选用二种可变电荷土壤粘粒(<2μ),分别含有0.35×10^-4-1.3×10^-4mol/L的不同电解质,在不同含水量下,在5—50℃范围内测量其直流电导率的变化。试验结果表明,电导热散法是研究土壤粘粒与离子相互作用的有用手段;电导率-温度曲线上的折点温度是随含水量、电解质种类和土壤类型而不同。在相同含水量下,含有不同电解质的红壤体系的折点温度具有如下的变化顺序:CaCl₂>Na₂SO₄>KCl>Ca(NO₃)₂>NaNO₃;砖红壤体系的折点温度明显高于红壤体系。折点温度的高低是土壤粘粒与离子相互作用强度的反映。     

坡面薄层水流流速测量的比较研究

在室内模拟水槽中分别用质心运动学原理、电解质脉冲法和流量法3种方法测量不同坡度、不同泥沙含量条件下的薄层水流流速。比较以上3种测量结果发现在下垫面无渗透时，即加入的盐液没有损失时，电解质脉冲法测量坡面薄层水流流速与质心运动速度及流量法测量结果基本是一致的。在泥沙含量较大时，电解质脉冲法测量结果的误差较大，流量对测量结果影响不显著；随着测量距离的延长，测量误差变小，这可能是随着测量距离的增加，加入电解质的时间与测量时间之比减小，从而使假设加入的电解质为电解质脉冲更加合理。总的来说，电解质脉冲法在实验条件下测量坡面薄层水流流速是可行的。     

A TITANIUM-RICH SOIL CLAY

A peaty podzol developed on glacial drift derived from chlorite-schists near Loch Awe, Argyll, contains up to 25 per cent titanium dioxide in the clay fractions after removal of organic matter and free iron oxides. Electron microscopy reveals that this titanium is almost entirely in the form of cryptocrystalline anatase which is amorphous to X-rays and which is removed by the HF method normally used to concentrate anatase and rutile in soils. The anatase has probably formed as a result of the weathering of sphene.     

MICROMORPHOLOGICAL QUANTIFICATION OF CLAY ILLUVIATION

Three concepts are introduced to describe the extent of clay illuviation phenomena quantitatively for pedogenic interpretations: (1) the degree of clay illuviation per thin section or (sub)horizon, subdivided into 5 classes, ranging from negligible (< 0.3 per cent by vol.) to very strong (> 7 per cent by vol.) clay illuviation; (2) the degree of reworking of the illuviated clay, subdivided into 3 classes, ranging from weak (< 30 per cent reworking) to strong (> 70 per cent); (3) the profile clay illuviation index: the sum of products of clay illuviation percentage per (sub)horizon and horizon thickness (in cm). The index ranges from very low (< 50 per cent cm) to very high (> 700 per cent cm). A distinction was made between the profile index based on the in situ illuviation features only and that based on all the illuviation features.     

DETECTION OF CLAY IN SOIL SOLUTION WITH METHYLENE-BLUE PAPER AND THE ASSESSMENT OF CLAY MOBILITY IN SOILS

The adsorption of methylene blue and the accompanying colour change appears to be a fairly specific and sensitive reaction for colloidal soil clay, especially when used with chromatography paper as a supporting medium. Thus minute amounts of clay in migrating soil solutions can be detected, and stability and electro-phoretic mobility of very dilute suspensions evaluated.     

MICROMORPHOLOGY OF SOME TROPICAL ALLUVIAL CLAY SOILS

The micromorphological properties of some marine and estuarine tropical clays from Holocene coastal plain soils of Surinam and Thailand have been explained against the background of sedimentation and initial soil formation. During geogenesis stratified sediments are formed, above which are sediments with slightly disturbed stratification, with or without matric faecal pellets. Pedogenesis during the sedimentation phase included development of channels in the sediment, formation of channel neostrians, biological homogenization, possibly pyrite accumulation, and partial oxidation and precipitation of iron as ferric hydroxide. During the brackish water phase pyrite accumulates in various amounts, mass illuviation may occur, part of the iron may oxidize and precipitate and part of the pyrite may be oxidized. During and after the swamp phase further oxidation and precipitation of iron as ferric hydroxide occurs, ferric hydroxide crystallizes into goethite. Pyrite becomes oxidized, resulting in the formation of jarosite, gypsum, silica, and ferric hydroxide.     

HYSTERESIS IN THE MOISTURE CHARACTERISTICS OF CLAY SOIL

The relation between soil suction, degree of saturation, and the air and water permeabilities is experimentally investigated for two clay soils. Marked hysteresis can exist between saturation and permeability, but does not follow a unique trend. Thus permeability can be greater on a wetting or drying cycle depending on the structure of the clay soil. This behaviour is considered in terms of the cluster concept of soil structure, and it is concluded that any general theory of hysteresis must recognize both the macrostructure and microstructure of a soil.     

INACTIVATION OF CLAY pH-DEPENDENT CHARGE IN ORGANO-MINERAL COMPLEXES

In 24 soils the CEC of untreated samples, of samples treated with hydrogen peroxide, and of samples treated with dimethyl sulphate, was determined at pH 3, S and 8. The CEC of clay and organic matter was calculated from multiple regression equations and compared with values after treatment with peroxide and after methylation. At pH 3 and pH 5 the CECs of clay by the three methods were similar, whereas at pH 8 they were significantly lower on untreated samples. The results are interpreted in relation to the formation of organo-mineral complexes and to the interaction of the acid functions of the clay and organic matter.