(Table 2) Calcium carbonate content in deep-sea surface sediments

The reconstruction of paleocarbonate ion concentrations provides an important constraint on the contribution of the CaCO3 cycle to the decrease in atmospheric CO2 content during glacial time. Such reconstructions have been challenging because each of the existing paleo-[CO3]2- indices has serious limitations. In this study, we reexamine the Broecker-Clark CaCO3 size index by analyzing the <20 µm, 20 to 38 µm, and 38 to 63 µm fractions in sediments from the Ontong-Java Plateau and the Ceara Rise. Scanning electron microscope analyses demonstrate that the less than 20 µm CaCO3 is dominated by coccoliths and the greater than 20 µm CaCO3 is dominated by foraminifera. Our results clearly indicate that the coccoliths are far more resistant to dissolution than the foraminifera. Referenced to a core top sample from 2.31 km depth in a core top sample from 4.04 km depth on the Ontong-Java Plateau, ~70% of the foraminifera CaCO3 was dissolved as opposed to only ~7% of the coccolith CaCO3. We found that the dissolution of foraminifera shells did not produce a significant amount of fragments smaller than 63 µm in size, and thus the Broecker-Clark size index is not a measure of the extent of fragmentation. Rather, it is a measure of the extent of differential dissolution of foraminifera relative to coccoliths. On the basis of these results, we propose a new dissolution index which involves the ratio of dissolution-susceptible foraminifera CaCO3 to total CaCO3.

Experimental data of CO2, CO3, Omega calcite saturation, pH values, alpha and epsilon fractionation factors, and Dd18O calctite-water

The oxygen isotopic composition (d18O) of calcium carbonate of planktonic calcifying organisms is a key tool for reconstructing both past seawater temperature and salinity. The calibration of paloeceanographic proxies relies in general on empirical relationships derived from field experiments on extant species. Laboratory experiments have more often than not revealed that variables other than the target parameter influence the proxy signal, which makes proxy calibration a challenging task. Understanding these secondary or "vital" effects is crucial for increasing proxy accuracy. We present data from laboratory experiments showing that oxygen isotope fractionation during calcification in the coccolithophore Calcidiscus leptoporus and the calcareous dinoflagellate Thoracosphaera heimii is dependent on carbonate chemistry of seawater in addition to its dependence on temperature. A similar result has previously been reported for planktonic foraminifera, supporting the idea that the [CO3]2- effect on d18O is universal for unicellular calcifying planktonic organisms. The slopes of the d18O/[CO3]2- relationships range between -0.0243 per mil/(µmol/kg) (calcareous dinoflagellate T. heimii) and the previously published -0.0022 per mil/(µmol/kg) (non-symbiotic planktonic foramifera Orbulina universa), while C. leptoporus has a slope of -0.0048 per mil/(µmol/kg). We present a simple conceptual model, based on the contribution of d18O-enriched [HCO3]- to the [CO3]2- pool in the calcifying vesicle, which can explain the [CO3]2- effect on d18O for the different unicellular calcifiers. This approach provides a new insight into biological fractionation in calcifying organisms. The large range in d18O/[CO3]2- slopes should possibly be explored as a means for paleoreconstruction of surface [CO3]2-, particularly through comparison of the response in ecologically similar planktonic organisms.

Raman spectroscopic study of the magnesium carbonate minerals– artinite and dypingite

Magnesium minerals are important in the understanding of the concept of geosequestration. The two hydrated hydroxy magnesium carbonate minerals artinite and dypingite have been studied by Raman spectroscopy. Intense bands are observed at 1092 cm-1 for artinite and at 1120 cm-1 for dypingite attributed CO32- ν1 symmetric stretching mode. The CO32- ν3 antisymmetric stretching vibrations are extremely weak and are observed at1412 and 1465 cm-1 for artinite and at 1366, 1447 and 1524 cm-1 for dypingite. Very weak Raman bands at 790 cm-1 for artinite and 800 cm-1 for dypingite are assigned to the CO32- ν2 out-of-plane bend. The Raman band at 700 cm-1 of artinite and at 725 and 760 cm-1 of dypingite are ascribed to CO32- ν2 in-plane bending mode. The Raman spectrum of artinite in the OH stretching region is characterised by two sets of bands: (a) an intense band at 3593 cm-1 assigned to the MgOH stretching vibrations and (b) the broad profile of overlapping bands at 3030 and 3229 cm-1 attributed to water stretching vibrations. X-ray diffraction studies show the minerals are disordered. This is reflected in the difficulty of obtaining Raman spectra of reasonable quality and explains why the Raman spectra of these minerals have not been previously or sufficiently described.

Synthesis and Raman spectroscopic study of Mg/Al,Fe hydrotalcites with variable cationic ratios

Hydrotalcites of formula Mg6 (Fe,Al)2(OH)16(CO3).4H2O formed by intercalation with the carbonate anion as a function of divalent/trivalent cationic ratio have been successfully synthesised. The XRD patterns show variation in the d-spacing attributed to the size of the cation. Raman and infrared bands in the OH stretching region are assigned to (a) brucite layer OH stretching vibrations (b) water stretching bands and (c) water strongly hydrogen bonded to the carbonate anion. Multiple (CO3)2- symmetric stretching bands suggest that different types of (CO3)2- exist in the hydrotalcite interlayer. Increasing the cation ratio (Mg/Al,Fe) resulted in an increase in the combined intensity of the 2 Raman bands at around 3600 cm-1, attributed to Mg-OH stretching modes, and a shift of the overall band profile to higher wavenumbers. These observations are believed to be a result of the increase in magnesium in the structure. Raman spectroscopy shows a reduction in the symmetry of the carbonate, leading to the conclusion that the anions are bonded to the brucite-like hydroxyl surface and to the water in the interlayer. Water bending modes are identified in the infrared spectra at positions greater than 1630 cm-1, indicating the water is strongly hydrogen bonded to both the interlayer anions and the brucite-like surface.

A Raman spectroscopic study of the uranyl mineral rutherfordine – revisited

The molecular structure of the uranyl mineral rutherfordine has been investigated by the measurement of the NIR and Raman spectra and complemented with infrared spectra including their interpretation. The spectra of the rutherfordine show the presence of both water and hydroxyl units in the structure as evidenced by IR bands at 3562 and 3465 cm-1 (OH) and 3343, 3185 and 2980 cm-1 (H2O). Raman spectra show the presence of four sharp bands at 3511, 3460, 3329 and 3151 cm-1. Corresponding molecular water bending vibrations were only observed in both Raman and infrared spectra of one of two studied rutherfordine samples. The second rutherfordine sample studied contained only hydroxyl ions in the equatorial uranyl plane and did not contain any molecular water. The infrared spectra of the (CO3)2- units in the antisymmetric stretching region show complexity with three sets of carbonate bands observed. This combined with the observation of multiple bands in the (CO3)2- bending region in both the Raman and IR spectra suggests that both monodentate and bidentate (CO3)2- units may be present in the structure. This cannot be exactly proved and inferred from the spectra; however, it is in accordance with the X-ray crystallographic studies. Complexity is also observed in the IR spectra of (UO2)2+ antisymmetric stretching region and is attributed to non-identical UO bonds. U-O bond lengths were calculated using wavenumbers of the 3 and 1 (UO2)2+ and compared with data from X-ray single crystal structure analysis of rutherfordine. Existence of solid solution having a general formula (UO2)(CO3)1-x(OH)2x.yH2O ( x, y  0) is supported in the crystal structure of rutherfordine samples studied.

The structure of selected magnesium carbonate minerals : a near infrared and mid-infrared spectroscopic study

The approach to remove green house gases by pumping liquid CO2 several kilometres below the ground implies that many carbonate containing minerals will be formed. Among these minerals the formation of dypingite and artinite are possible; thus necessitating a study of such minerals. Two carbonate bearing minerals dypingite and artinite with a hydrotalcite related formulae have been characterised by a combination of infrared and near-infrared spectroscopy. The infrared spectra of both minerals are characterised by OH and water stretching vibrations. Both the first and second fundamental overtones of these bands are observed in the NIR spectra in the 7030 to 7235 cm-1 and 10490 to 10570 cm-1. Intense (CO3)2- symmetric and antisymmetric stretching vibrations confirm the distortion of the carbonate anion. The position of the water bending vibration indicates water is strongly hydrogen bonded to the carbonate anion in the mineral structure. Split NIR bands at around 8675 and 11100 cm-1 indicates that some replacement of magnesium ions by ferrous ions in the mineral structure has occurred.

Thermal analysis of hydrotalcite synthesised from aluminate solutions

The aluminate hydrotalcites are proposed to have either of the following formulas: Mg4Al2(OH)12(CO3 2-)·xH2O or Mg4Al2(OH)12(CO3 2-, SO4 2-)·xH2O. A pure hydrotalcite phase forms when magnesium chloride and aluminate solns. are mixed at a 1:1 volumetric ratio at pH 14. The synthesis of the aluminate hydrotalcites using seawater results in the formation of an impurity phase bayerite. Two decompn. steps have been identified for the aluminate hydrotalcites: (1) removal of interlayer water (230 °C) and (2) simultaneous dehydroxylation and decarbonation (330 °C).

Infrared and Raman spectroscopic characterization of the carbonate mineral huanghoite - and in comparison with selected rare earth carbonates

Raman spectroscopy complimented with infrared spectroscopy has been used to study the rare earth based mineral huanghoite with possible formula given as BaCe(CO3)2F and compared with the Raman spectra of a series of selected natural halogenated carbonates from different origins including bastnasite, parisite and northupite. The Raman spectrum of huanghoite displays three bands are at 1072, 1084 and 1091 cm−1 attributed to the symmetric stretching vibration. The observation of three symmetric stretching vibrations is very unusual. The position of symmetric stretching vibration varies with mineral composition. Infrared spectroscopy of huanghoite show bands at 1319, 1382, 1422 and 1470 cm−1. No Raman bands of huanghoite were observed in these positions. Raman spectra of bastnasite, parisite and northupite show a single band at 1433, 1420 and 1554 cm−1 assigned to the ν3 (CO3)2− antisymmetric stretching mode. The observation of additional Raman bands for the ν3 modes for some halogenated carbonates is significant in that it shows distortion of the carbonate anion in the mineral structure. Four Raman bands for huanghoite are observed at 687, 704, 718 and 730 cm−1and assigned to the (CO3)2− ν2 bending modes. Raman bands are observed for huanghoite at around 627 cm−1 and are assigned to the (CO3)2− ν4 bending modes. Raman bands are observed for the carbonate ν4 in phase bending modes at 722 cm−1 for bastnasite, 736 and 684 cm−1 for parisite, 714 cm−1 for northupite. Raman bands for huanghoite observed at 3259, 3484 and 3589 cm−1 are attributed to water stretching bands. Multiple bands are observed in the OH stretching region for bastnasite and parisite indicating the presence of water and OH units in their mineral structure. Vibrational spectroscopy enables new information on the structure of huanghoite to be assessed.

A Raman spectroscopic comparison of calcite and dolomite

Raman spectroscopy was used to characterize and differentiate the two minerals calcite and dolomite and the bands related to the mineral structure. The (CO3)2− group is characterized by four prominent Raman vibrational modes: (a) the symmetric stretching, (b) the asymmetric deformation, (c) asymmetric stretching and (d) symmetric deformation. These vibrational modes of the calcite and dolomite were observed at 1440, 1088, 715 and 278 cm−1. The significant differences between the minerals calcite and dolomite are observed by Raman spectroscopy. Calcite shows the typical bands observed at 1361, 1047, 715 and 157 cm−1, and the special bands at 1393, 1098, 1069, 1019, 299, 258 and 176 cm−1 for dolomite are observed. The difference is explained on the basis of the structure variation of the two minerals. Calcite has a trigonal structure with two molecules per unit cell, and dolomite has a hexagonal structure. This is more likely to cause the splitting and distorting of the carbonate groups. Another cause for the difference is the cation substituting for Mg in the dolomite mineral.

Raman and infrared spectroscopic study of kamphaugite-(Y)

We have studied the carbonate mineral kamphaugite-(Y)(CaY(CO3)2(OH)·H2O), a mineral which contains yttrium and specific rare earth elements. Chemical analysis shows the presence of Ca, Y and C. Back scattering SEM appears to indicate a single pure phase. The vibrational spectroscopy of kamphaugite-(Y) was obtained using a combination of Raman and infrared spectroscopy. Two distinct Raman bands observed at 1078 and 1088cm(-1) provide evidence for the non-equivalence of the carbonate anion in the kamphaugite-(Y) structure. Such a concept is supported by the number of bands assigned to the carbonate antisymmetric stretching mode. Multiple bands in the ν4 region offers further support for the non-equivalence of carbonate anions in the structure. Vibrational spectroscopy enables aspects of the structure of the mineral kamphaugite-(Y) to be assessed.

Near infrared spectroscopy of selected natural magnesium carbonates: implications for geosequestration

The approach to remove greenhouse gases by pumping liquid CO2 several kilometres below the ground implies that many carbonate containing minerals will be formed. Among these minerals, the formation of hydromagnesite, dypingite and nesquehonite are possible, thus necessitating a study of such minerals. These minerals with a hydrotalcite-related formulae have been characterised by a combination of infrared and near infrared spectroscopy. Layered double hydroxides (also known as anionic clays or hydrotalcites) are a group of layered clay minerals described by the general formula: [M1–x2+Mx3+(OH)2]x+[An–]x/n∙mH2O. The infrared spectra of the minerals are characterised by OH and water stretching vibrations. Both the first and second fundamental overtones of these bands are observed in the NIR spectra in the 7030–7235 cm–1 and 10,490–10,570 cm–1 spectral ranges. Intense (CO3)2– symmetrical and anti-symmetrical stretching vibrations confirm the distortion of the carbonate anion. The position of the water bending vibration indicates water is strongly hydrogen-bonded to the carbonate anion in the mineral structure. NIR spectroscopy offers a method for quickly analysing such materials.

海相碳酸盐－稀土元素共沉淀过程中的分异作用研究

本文主要运用稳定加液－反应系统对海水中方解石和文石形成时稀土元素的共沉淀现象进行了分析，研究了稀土元素在固-液体系中的迁移、转化和分配。进而在对其定量描述的前提下，研究了稀土元素共沉淀对各种反应条件的响应，并对共沉淀行为的机制进行了探讨。 本实验首先运用pH测试、高精度滴定分析等手段测定了实验中的一些基本参数，如[H+]、碱度和[Ca2+]，根据计算结果获得了各碳酸体系要素，并以此为基础建立了5℃、15℃和25℃及pCO2=0.003atm下海水中方解石或文石的沉淀动力学方程。实验结果表明： 1）在各条件下，方解石或文石的沉淀速率（R）和其在海水中过饱和度（Ω）存在很好的线性相关性，即海相碳酸盐的沉淀动力学方程可以通过下面的基本表达式来表示：LogR=k*Log(Ω-1)+b ； 2）过高的稀土元素浓度会对文石或方解石的沉淀产生抑制作用，进而对共沉淀过程中YREEs的分异和分馏产生一定的影响。相比方解石而言，文石的沉淀动力学过程承受稀土元素的干扰能力更强； 3）不同温度下得到的方解石或文石各自的沉淀动力学方程存在明显的差异，表明这一过程受热力学因素控制。相对于方解石而言，温度对文石的沉淀动力学的影响更为显著。 与前人研究不同的是，本实验中YREEs的浓度设定在非常低的范围内，从而避免了过高浓度YREEs对方解石或文石沉淀动力学过程的干扰。在最终的反应液中，各种实验条件非常接近自然环境。有关稀土元素的共沉淀行为主要得出以下定性或定量化结论： 1）YREEs在随方解石或文石的共沉淀过程中，均发生了强烈的分异作用。在方解石实验中，稀土元素的分异系数分布曲线呈凸状分布；而在文石实验中，稀土元素的分异系数随原子序数的增加逐渐减小，遵循镧系收缩的规律。总的来说，稀土元素，尤其轻稀土元素在文石中的分异作用要强于方解石。 2）无论是方解石还是文石，沉淀速率对YREEs的分异作用都有着明显的影响。在方解石中，YREEs的分异系数随沉淀速率的增加呈一致性递减趋势；而在文石中，其分异系数对文石沉淀速率有着截然不同的响应：轻稀土元素（La, Ce, Nd, Sm, Eu, Gd）的分异系数随文石沉淀速率的增加而下降，而重稀土元素（Ho, Y, Tm, Yb , Lu）的分异系数则随文石沉淀速率的增加呈上升趋势。 3）在方解石中YREEs的分异系数之间存在非常好的相互关系，表明这些元素是以成比例的方式参与共沉淀。整个谱系呈现中等强度的分馏，MREE相对于LREE和HREE要更为富集；在文石中由于沉淀速率的作用不同，只有Y、Ho、Yb、Lu等元素的分异系数之间有较好的相互关系。YREEs出现了差异性的强烈分馏，在新生成沉淀中轻稀土元素相对于重稀土元素强烈富集。 4）YREEs在溶液中和碳酸盐晶体表面的碳酸根配位形式对YREEs在共沉淀过程中的分异作用极为重要，YREEs在碳酸盐晶体表面的吸附是整个谱系发生分馏效应的关键环节。对于文石来讲，晶体中有效YREE离子和Ca离子半价大小之间的相近程度是其分馏效应的关键因素；而对于方解石来说，YREEs在方解石晶格中的安置就是其分馏效应的关键控制因子，但在晶格安置中起到关键作用的是YREEs和方解石中O原子之间离子键M-O的键长，而非离子半径。 5）综合YREEs在方解石中的分异作用和分馏效应，我们认为M2(CO3)3-CaCO3和MNa(CO3)2-CaCO3是最为可能的两种固体溶液形成模式。 最为重要的是，对比我们的实验结果与前人在灰岩、叠层石、微生物成因碳酸盐等方解石质载体中的研究成果，两者之间出现了非常好的一致性。我们认为方解石质载体将是重建古海水中稀土元素相关信息的重要工具。相比之下，文石质载体不适合作为类似的载体。

水热条件下钾长石碱性分解反应机理的实验研究

It is well known that our country is short of water-soluble potassium, but rich in insoluble potassium ores. Based on the work of the formers, using the orthogonal and monofactor experiments, the author optimized the production technology of micro-porous potassium silicon calcium mineral fertilizer by non-stirring hydrothermal chemical reaction when the alkaline earth booster CaO was available. The influences of temperature、time、reactant ratio and water-solid ratio on the dissolution rate of production’s elements were studied by orthogonal experiments, and the production technology was further optimized by monofactor experiments. By XRD、SEM、EDS and dissolving experiments, it was systematically studied that the effects of the reactant ratio、reaction time and reaction temperature on the properties of the production obtained by the hydrothermal reaction between KAlSi3O8 and CaO. The results showed that：when changing of the reaction condition, the reaction productions included tobermorite、 hibschite、α-C2SH and K2Ca(CO3)2; among which, K2Ca(CO3)2 was not the first production containing potassium, but K2Ca(CO3)2 was synthesized by the reaction among KOH、Ca(OH)2 and CO2. Whether the phase was synthesized was related to not only the reaction condition, but also their physicochemical properties; when the reaction condition was changed, the changes of different phases were different. The results of XRD and dissolution rate experiments explained the dissolution characteristic of every element of hydrothermal productions very well, and the relation between the dissolution rate of element and the phase of productions poured a good illumination on the production technology. The results of SEM and EDS showed that: hydrogarnet looked like spherical, and its surface was covered by some productions including K phase and Ca、Si phase; but the morphology of tobermorite was platy or lamellar or needlelike, and parts of Si in the structure of tobermorite were substituted by Al，and some K+ cations were inserted into the Ca interlayer of tobermorite at the same time. It was the first time that the interface between KAlSi3O8 and Ca(OH)2 was observed directly by SEM and EDS after the hydrothermal reaction, and the mechanism of hydrothermal reaction of KAlSi3O8 and Ca(OH)2 was further discussed. These results indicated that: the Ca-KAlSi3O8 intermediate compound was formed at first, and some K was released into the solution and KOH was produced at the same time; the C-S-H phase appeared before hydrogarnet, and then hydrogarnet was synthesized when the chemical reaction was carried on; if the reaction was carried on furthermore, α-C2SH、tobermorite and other C-S-H phases of different atom ratio appeared. The author found that the structure of KAlSi3O8 would be more drastically destroyed if there were some reactants, such as Ca(OH)2 which reacted with KAlSi3O8 and new phases were formed after the hydrothermal reaction between KAlSi3O8 and alkaline solution of equal ionic strength was finished. With the combination of calcination and hydrothermal reaction methods, the dissolution rate of products were greatly improved when the hydrothermal reaction was carried out after KAlSi3O8 and CaCO3 were calcined. Furthermore, the author has tentatively explored how to evaluate the effects of the differences of the activity of lime on the dissolution properties of hydrothermal products.

巢湖、龙感湖水体中稀土元素的无机形态研究

运用MINTEQ 化学平衡软件对巢湖、龙感湖中溶解态稀土的形态进行模拟。模拟结果表明, 在巢湖和龙感湖中Ln (CO3) 2- , LnCO3+ 是溶解态稀土的最主要的存在形式, 当8 > pH > 7. 19 时, REE 主要以LnCO3+ 形式存在, 当pH > 8 时, REE 主要以Ln (CO3) 2- 形式存在, 并且ΣLn (CO3) n3 - 2 n ( n = 1 和2) 形态的稀土基本上占溶解态稀土总含量的93 %以上。Ln3 + 在巢湖和龙感湖水体中平均丰度为5. 03 % , Ln3 + 的丰度和pH 值成反相关关系。LnPO4 在湖水中平均丰度为1. 61 % , 但这种形式的稀土在巢湖和龙感湖中非常重要。巢湖和龙感湖中LREE 的LnPO4 均处于过饱和状态, 甚至巢湖西半湖区丰水期HREE 的LnPO4 的也都处于过饱和状态, PO43 - 对稀土的存在有很强的限制作用。LnSO4 , LnF2 + , LnOH2 + , LnCl2 + 等形态的各元素平均丰度均小于1 % , 在富营养化的淡水中通常可以忽略不计。

溶液介质条件和腐殖影响下REE在水/粘土界面分配和分馏的实验研究

过去几十年，由于REE具有重要的物源和过程示踪的地球化学意义，又与核放射性元素（钢系元素）的地球化学结构类似，因此，稀土元素的表生地球化学分配和行为研究便成为微量元素地球化学研究的一个重要部分。目前"通过水体悬浮物吸附态REE组成变化分析研究水／微粒界面作用REE分异现象．的工作不少，但至今进行的胶体或其他微粒吸附REE的实验研究不多，且已有的实验未能对溶液介质条件（如pH、离子强度、阴离子、固／液比），尤其是天然有机物的控制机理进行系统研究，对所观察到的水体中REE及其他微量元素分布变化多样性的解释仍缺乏实验依据。本文用结晶良好且粘土矿物含量高的苏州高岭土、美国粘土协会高岭土（Kga-1b）和蒙脱土（Wwy-2）作为吸附剂，采用系列吸附实验定量研究了不同理化条件（如pH值、离子强度、固／液比）下，受溶液阴离子（Cl-、C1O4-、SO42-、HCO3-）和Fluka胡敏酸（HA）影响，REE在粘土／水界面的分配和分馏，并讨论了HA和粘土的相互作用及胡敏酸存在与不存在时的REE形态分布。得到以下几点重要认识，为合理解释地表水体中既E和其他微量元素分布变化的多样性提供了实验依据：1、REE在苏州高岭土／水界面的重现性实验结果为：稀土配分系数D的相对标准偏差最大值为Eu8.4％，其他大多介于5．0％和6．6％间。而稀土吸附率Rd的相对标准偏差最大值为D2.2％，其他大多＜2％。较小误差表明本次研究所用实验方法是可行的。2、REE在苏州高岭土／水界面的动力学实验结果表明：短时间内（几分钟）稀土快速吸附在高岭土：接着因为粘土的层状结构，在20h内粘土层间金属与REE发生交换，稀土分配系数变化较大；20h以后能达到稳定的吸附／解吸平衡。因此本次研究采用的平衡时间为24h。3、pH分别为4.5和6.5时REE在苏州高岭土冰界面的分配能用Langmuir吸附等温线模拟和MINEQL＋软件表达。与静电吸附相对应，pH值越高REE最大吸附量越大。同时REE浓度的差异造成了REE分馏，总的趋势是REE含量越高，分馏越不明显。4、近中性（pH＝6.5）条件下不同阴离子的存在对REE在苏州高岭土／水界面分配和分馏的影响表明：随阴离子（Cl-、ClO4-、SO42-）含量升高REE吸附率降低，其中SO42-对REE吸附的影响最大，说明Na＋质量效应和阴离子配合的影响；同时由于不同阴离子与轻重R陇的络合差异所致，阴离子含量越高，轻重稀土的分馏越明显（La／Yb＝0.14-0.96），一般为阴离子含量的增加使得重稀土更多的被吸附，其中C1-和SO42+的影响最为明显。HCO3-虽然与REE有较强配合，但可能由于我们的HCO3-实验浓度低（＜0.0O25mol／L），在我们的实验结果中其对REE吸附和分馏的影响较小。5、由于不同pH和介质条件下，REE的络合形态分布不同，它们可以影响其在水／粒界面的分配。应用MINEQL＋模型，考虑REE的氢氧化物、碳酸盐和腐殖酸的影响，研究了REE的形态分布，结果表明fIA的存在对REE形态有很大影响：在HA不存在时，pH7-8间REECO3＋为主要的REEs形态，在更低和更高pH值，REE主要存在形式分别为REE加和REE（CO3）2-；而当HA存在时，在1）H值3-9，REEHA成为主要形态，在低pH（＜3）和高pH（＞9）时REE3+和REE（CO3）2-分别为主要形态。6、在较宽的pH范围HA能吸附在粘土上意味着在大多数含HA的天然水体中，粘土表面被HA覆盖。随H增加粘土对HA的吸附降低，反应了配位体交换或表面络合反应引起的专属吸附，其他如疏水性、、腐殖物质的溶解和HA的结构变化可能也影响了吸附。HA含量、矿物表面积和离子强度等理化条件对HA吸附会产生影响，从而影响HA对粘土表面的覆盖和接下来的粘土对REE的吸附。7、溶液介质条件对REE在粘土（Kga-1b和SWy-2）／水界面分配和分馏的影响表明：主要与静电相互作用、离子交换反应相对应，除低PH外，REE在高岭土上的吸附表现出弱的pH依赖性；而随pH增加REE在蒙脱土上的吸附呈下降趋势，显示交换反应为吸附过程的主要因素。在两种粘土中REE吸附均为随离子强度增加而降低，反应了Na质量效应。8、腐殖物质在粘土表面的吸附改变了吸附剂的属性。HA存在时REE在固液界面的分配反应了REEHA在固液界面的分配和HA在高岭土或蒙脱土／水界面上的分配，其他如静电吸附等机制也影响了吸附：在高岭土中，HA会增加低pH（＜4）吸附，随pH增加（＞5）HA会降低吸附。与此不同，在整个PH范围（3-10），HA的存在明显降低了REE在蒙脱土上的吸附。REE吸附在高岭土上随队含量增加是先增加后降低。而蒙脱土实验中，在低HA含量（＜5mg／L）处，RE阮吸附率与HA含量增加呈线性降低至几个百分比，而在高队含量处，REEs吸，附率无明显变化。这些清楚地说明水体环境中有机物的存在通常降低微量金属吸，附在微粒上，增加微量金属在水体中的溶解量，从而促进微量金属在水体环境中的长距离迁移。9、HA存在和不存在时，吸附／解吸过程中的REE分馏随pH或离子强度的变化都不明显，但由于REE系列与腐殖物质和矿物络合的差异，会随队含量的变化发生明显变化。通常溶液中高队含量增加了LREE在高岭土／蒙脱土上的吸附。这些结果是在HA存在时，微粒相上产生LREE富集的一个实验证实，也和大多数天然水体中的REEs分馏相一致。