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较浅
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  relative shallow
     ( 4 ) The making of secondary pores may be formed in relative shallow depth due to higher geotemperature.
     4高地温能加快有机质的成熟 ,从而有利于次生孔隙在较浅的深度形成。
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     in the process of rain,the critical slip surface changes from deep surface to relative shallow surface,in the process of evaporation,the situation is opposite.
     降雨过程中边坡的临界滑动面由较深位置向较浅位置转变,蒸发过程则相反。
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  “较浅”译为未确定词的双语例句
     About 64.78%(4 663.53×10~8 tons) resources are buried from the depth of 0 m to 500 m and 35.22%((2 535.86)×10~8 tons) were buried between the depth of 500 m to 1 000 m.
     我国油页岩埋藏深度较浅,埋深在0~500 m之间的油页岩资源为4 663.51亿t,埋深在500~1 000 m之间的油页岩资源为2 535.86亿t,分别占全国油页岩资源的64.78%和35.22%。
短句来源
     Thermally stimulated depolarization current (TSDC) results indicate that there are two types of shallow traps in the composite, 0.52eV and 0.62eV with trap densities 1.2×1010/cm3 and 2.0×1011/cm3, which differs significantly from that of pure SP (0.58eV, 3.1×1010/cm3).
     采用热刺激退极化电流(TSDC)测量的结果表明纳米复合材料中存在两个较浅的陷阱能级,分别为0.52eV和0.62eV,陷阱密度分别为1.2×1010/cm3和2.0×1011/cm3,与纯SP中浅陷阱深度0.58eV、陷阱密度3.1×1010/cm3明显不同。
短句来源
     68%, 29% and 25% in the deep infiltrated tissues, 19%, 31% and 25% in the low infiltrated tis sues.
     浸润程度较深的组织 68%、2 9%和 2 5 % ,浸润程度较浅的组织 19%、31%和 2 5 %。
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     The results show that the ground state of HeNa is unstable , the state 2Π3p has a shallow potential well as well as the state 1Π2p of HeNa+ and the states of 3∑3s and 1∑3s of the cation have very deep potential wells.
     结果说明HeNa分子的基态是不稳定的,激发态2∏3p有一个较浅的势阱,HeNa~+的1∑2p有一个较浅的势阱,而~3∑3s态及~t∑3s态分别存在一个很深的势阱.
短句来源
     Results:Serosa of most cases was not involved and29.8%(31/104)of cases were early gastric cancer.
     结果:淋巴结转移阴性胃癌浸润深度较浅,其中近29.8%为早期胃癌(31/104)。
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  相似匹配句对
     coal-beds are shallowly buried;
     煤层埋藏 ;
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     The sand buried shallowly may be liquefaction.
     埋藏的砂土会发生液化。
短句来源
     Superficial View of Electronic Commerce
     论电子商务
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     Superficial view of loci of Qi
     气穴
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     Complications were rare.
     并发症少见。
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  relative shallow
Due to relative shallow areas close to the inlet throat and large grain sizes, the current velocities are quite high.
      


In this work the oxidation reactions of quinazolone-4 with chromic acid, potassium permanganate, peracetic acid, and perbenzoic acid have been studied. When quinazolone was heated with chromic anhydride in glacial acetic acid, quinazolone chromate(I) was isolated as previously reported in literature. Oxidation of quinazolone with potassium permanganate in neutral or alkaline solutions gave quinazolone oxalate (III) and with the same reagent in acidic solutions produced benzoylene urea (2,4-dihydroxyquinazoline,...

In this work the oxidation reactions of quinazolone-4 with chromic acid, potassium permanganate, peracetic acid, and perbenzoic acid have been studied. When quinazolone was heated with chromic anhydride in glacial acetic acid, quinazolone chromate(I) was isolated as previously reported in literature. Oxidation of quinazolone with potassium permanganate in neutral or alkaline solutions gave quinazolone oxalate (III) and with the same reagent in acidic solutions produced benzoylene urea (2,4-dihydroxyquinazoline, II). Carbon dioxide and ammonia were always liberated in these experiments, but no other oxidation product was isolated.In the oxidation with hydrogen peroxide in glacial acetic acid or in acetic anhydride, the following five compounds have been isolated and identified, namely, N~1, N~3-quinazolone dioxide (IV), 2,4,6-trihydroxyquinazoline (V), N-formyl-o-nitrobenzamide (VI), o-nitrobenzamide (VII) and benzoic acid (VIII). The relative amount of these products varied with the conditions of th oxidation reaction. Thus, when the reaction was carried out in glacial acetic acid at 55—60° for 14—28 hours, quinazolone was oxidized predominantly to compound VI (48—63% ), VII (11—17%) and VIII (3—9%). But when the oxidation was carried out at lower temperature (15—25°) either in glacial acetic acid or in acetic anhydride, the principal products were IV (up to 65%), V(up to 11%) and VI (up to 22%), and no significant amount of compounds VII and VIII could be obtained. From the reaction of quinazolone with perbenzoic acid in chloroform, the only product isolated was compound IV (51%).The oxidation products benzoylene urea (II) and benzoic acid (VIII) were identified by means of the mixed melting points. Quinazolone oxalate (III) was identified through its mixed melting point and the isolation of quinazolone and oxalic aicd upon treatment with sodium bicarbonate and followed by calcium chloride. The identity of o-nitrobenzamide (VII) was established through its mixed melting point and its hydrolysis o-nitrobenzoic acid.The structure of N-formyl-o-nitrobenzamide (VI) has been elucidated from its composition, its inability to react with potassium iodide, a characteristic reaction of N-oxide, and its easy hydrolysis in boiling water, cold dilute sodium bicarbonate solution and moist pyridine to o-nitrobenzamide and formic acid. The structure of quinazolone di-N-oxide(IV) has been determined on the basis of its elementary analysis, its conversion into quinazolone by potassium iodide in acetic acid at room temperature, its rearrangement to 2, 4,6-trihydroxyquinazoline in glacial acetic acid at 120° or with phosphorus trichloride in chloroform, and its further oxidation by hydrogen peroxide in glacial acetic acid to o-nitrobenzamide.The structural formula of 2,4,6-trihydroxyquinazoline (V) has been established by the following facts: First, its composition was found to be the same as the quinazolone di-N-oxide from which it was derived, but unlike the latter, it did not react with potassium iodide. Secondly,this compound gave a deep violet color with ferric chloride solution and formed with acetic anhydride a monoacetyl derivative which gave no color reaction with ferric chloride solution but could be hydrolyzed by diluted hydrochloric acid to the original trihydroxyquinazoline. Thirdly, the trihydroxyquinazoline reacted with phosphorus pentachloride in phosphorus oxychloride to give 2,4,6-trichloroquinazoline, and the latter was converted by hydrolysis with concentrated hydrochloric acid to 2,4-dmydroxy-6-chloroquinazoline. The identities of these monochloro-and trichloro-compounds have been established by mixed melting points with synthetic samples.Based upon the facts mentioned above, the mechanism of the oxidative degradation of quinazolone-4 with hydrogen peroxide in glacial acetic acid to form compounds IV—VII has been proposed as follows:The mechanism of the formation of benzoic acid (VIII) is still obscure.

喹唑酮在冰醋酸中与三氧化铬作用,形成喹唑酮铬酸盐(I);在中性或硷性溶液中与高锰酸钾作用,形成喹唑酮草酸盐(III),但在酸性溶液中与高锰酸钾作用,则形成2,4-二羟基喹唑啉(II)。以过氧化氢在冰醋酸或醋酸酐中与喹唑酮作用,分离出N~1,N~3-二氧化喹唑酮(IV),2,4,6-三羟基喹唑啉(V),N-甲酰隣硝基苯甲酰胺(VI),隣硝基苯甲酰胺 (VII)及苯甲酸(VIII)等化合物。这些氧化产物的相对产量,随反应条件不同而有很大的差别。在较强烈的条件下,主要产物为氧化程度较高的衍化物(VI—VIII);而在较温和的条件下,则主要产物为氧化程度较浅的化合物(IV—VI)。以过氧化苯甲酸在氯仿中与喹唑酮作用,则只分离出IV。 N~1,N~3-二氧化喹唑酮在醋酸中以碘化钾脱氧得到喹唑酮;在醋酸中重排为2,4,6-三羟基喹唑啉;在冰醋酸中与过氧化氢进一步反应,则得隣硝基苯甲酰胺。2,4,6-三羟基喹唑啉与醋酸酐作用,可得2,4二羟基-6-乙酰氧基喹唑啉,后者水解又得到三羟基喹唑啉。2,4,6-三羟基喹唑啉与五氯化磷在三氯氧磷中作用,即氯化为2,4,6-三氯喹唑啉,后者水解则得到2,4-二羟基6-氯喹唑...

喹唑酮在冰醋酸中与三氧化铬作用,形成喹唑酮铬酸盐(I);在中性或硷性溶液中与高锰酸钾作用,形成喹唑酮草酸盐(III),但在酸性溶液中与高锰酸钾作用,则形成2,4-二羟基喹唑啉(II)。以过氧化氢在冰醋酸或醋酸酐中与喹唑酮作用,分离出N~1,N~3-二氧化喹唑酮(IV),2,4,6-三羟基喹唑啉(V),N-甲酰隣硝基苯甲酰胺(VI),隣硝基苯甲酰胺 (VII)及苯甲酸(VIII)等化合物。这些氧化产物的相对产量,随反应条件不同而有很大的差别。在较强烈的条件下,主要产物为氧化程度较高的衍化物(VI—VIII);而在较温和的条件下,则主要产物为氧化程度较浅的化合物(IV—VI)。以过氧化苯甲酸在氯仿中与喹唑酮作用,则只分离出IV。 N~1,N~3-二氧化喹唑酮在醋酸中以碘化钾脱氧得到喹唑酮;在醋酸中重排为2,4,6-三羟基喹唑啉;在冰醋酸中与过氧化氢进一步反应,则得隣硝基苯甲酰胺。2,4,6-三羟基喹唑啉与醋酸酐作用,可得2,4二羟基-6-乙酰氧基喹唑啉,后者水解又得到三羟基喹唑啉。2,4,6-三羟基喹唑啉与五氯化磷在三氯氧磷中作用,即氯化为2,4,6-三氯喹唑啉,后者水解则得到2,4-二羟基6-氯喹唑啉。 N-甲酰隣硝基苯甲酰胺与沸水,冷碳酸氢钠水溶液或湿吡啶作用,则水解为隣硝基苯甲酰胺及甲酸。根据我们实验的结果,这些氧化产物的生成机构如下:■

After soil survey of the whole region,it is found that the soils of the North China Great Plain consist of four great soil groups including drab soil,light meadow soil,glei swamp soil and saline soil.The term“calcareous alluvial soils” formerly used hardly interprets any mean of soil formation and productive cha- racteristics. The drab soils formerly named as“Shangtung brown soils”are generally located on the alluvial fan and the foot of mountains.Owing to the higher relief,excess drainage and deeper ground...

After soil survey of the whole region,it is found that the soils of the North China Great Plain consist of four great soil groups including drab soil,light meadow soil,glei swamp soil and saline soil.The term“calcareous alluvial soils” formerly used hardly interprets any mean of soil formation and productive cha- racteristics. The drab soils formerly named as“Shangtung brown soils”are generally located on the alluvial fan and the foot of mountains.Owing to the higher relief,excess drainage and deeper ground water(below 4—6 meters),saliniza- tion is not found.The drab soil is neutral to slightly alkaline in reaction. The chemical data show no evidence of chemical decomposition of clay,but the disintegration of soil particles-clay formation is quite obvious.Along the foot of Taihang range,the drab soils are covered with new calcareous material and bring out the process of recalcification shown by the presence of pseudo- mycelins in the Soil profiles. Light meadow soils are generally distributed in the alluvial plain with higher ground water table laying at 2—3 meters.Owing to the frequency of the fluc- tuation of the ground water in the soil profile,oxidation and reduction are alternately carried out and lots of rusts and mottlings are found in the soil profile of these soils.Under intensive cultivation,the surface soil of light meadow soil is usually loose and mellow and contains lower content of organic matter. The glei swamp soils are formed by the lakeside and in the depressed lowlands where ground water table is quite shallow and sometimes close up to the sur- face.In the depressed lands contacted with mountain foot,longer duration of water-lodging produces strongly gleyed swamp soil with higher content of humus. In the depressed portion of alluvial plain,the temporary water-lodging gives weakly gleyed swamp soil with low content of humus,whilst the strongly gleyed soils are found in the depressed land along seacoast. Salinization of soils is influenced by the ground water and relief.Saline soils are usually distributed in the lowland with higher ground water table and higher mineral content of the water.Irrigation without drainage system will rise ground water table and causes the process of secondary salinization. Saline soils of North China plain may be divided into two subtypes:(1) Saline soil of alluvial plain and(2)Saline soils along the seacoast.The former belongs to the chloride-sulfate saline soils in which the ground water table is about 1.5—2.0 meters and the mineral content of the ground water is about 1—3 grams/liter.In the coastal region,the chloride saline soils are usually found with high ground water table at 1.0—1.5 meter and also high mineral content more than 10 grams/liter.The transitional belt between these two soils above-mentioned is sulfate-chloride saline soils where the ground water table is around 1.5 meter and the mineral content of ground water is 5—10 grams/liter. These four genetic soil types are closely related each other and also alternate between themselves.It is very interesting to study the transitional types among these four soil groups. Between drab soils and light meadow soils,the transitional soil types as meadow drab soils and drab meadow soils are formed under different transitional circumstances.The meadow drab soil is distributed at the bottom of alluvial fan with higher ground water table(1.5—3 meters),while the drab meadow soil is formed on the old riverbed in the alluvial plain with comparatively uplifting relief where the ground water table becomes deeper(3—3.5 meters). Many transitional soil types are also developed between the light meadow soils and glei swamp soils.The worse water lodging condition enforces the meadow soil transfering to glei swamp soil,whilst promotion of water condi- tion by diking drainage cannel or local silting up of lowlands causes the trans- formation of glei swamp soil in to light meadow soil or even to the drab soil. Salinization of soil is always accompanied with the formation of light meadow soil.Rising the ground water table and increasing the mineral content of ground water will induce or enforce the process of sainization of soils.On the other side,desalinization of soils can be carried out when the ground water table becomes lower.When the seatide is shut by dikes and the drainage condition is improved,the saline soil in the coastal region will be transfered to the light meadow soils.

经过一年多的大规模调查,证实了华北平原的土壤都具有不同的类型和不等程度的发育,其中包括很多土类、亚类和变种,过去简称华北平原土壤为“石灰性冲积土”,是很难反映情况和说明问题的。华北平原的主要成土过程有褐土过程、浅色草甸土过程、沼泽过程和盐土过程。褐土多发育于山麓及冲积扇形地上,地势较高,排水良好,地下水埋藏较深,约在4—6米以下。在降水淋洗之下,可溶盐类皆被淋失,不发生盐演化现象,土壤只及于粘化作用,pH 值多属中性至微碱性。太行山麓的褐土因受石灰性沉积物的覆盖,发生次生碳酸盐化作用,土壤剖面中有假菌丝体存在。浅色草甸土多分布于冲积平原,其形成过程受地下水的影响极显著。地下水埋藏深度约2—3米,也可达4—5米。由于地下水升降频繁,氧化还原作用交替进行,土壤中呈现显明的锈纹斑,但无假菌丝体。土壤疏松多孔而有结构性,因土壤中有机质较少、土色浅淡而多受人为耕作的影响,故称耕种浅色草甸土。洼地及湖淀附近,地下水埋藏较浅或地表积水,土壤发生沼泽化过程。山麓交接洼地,积水时期长久,潜育作用及腐殖质积累均较显著。平原中洼地比较平坦,积水时间亦较短,腐殖质积累和潜育作用都较轻微。海滨洼地中,潜育作用较为剧烈,但有...

经过一年多的大规模调查,证实了华北平原的土壤都具有不同的类型和不等程度的发育,其中包括很多土类、亚类和变种,过去简称华北平原土壤为“石灰性冲积土”,是很难反映情况和说明问题的。华北平原的主要成土过程有褐土过程、浅色草甸土过程、沼泽过程和盐土过程。褐土多发育于山麓及冲积扇形地上,地势较高,排水良好,地下水埋藏较深,约在4—6米以下。在降水淋洗之下,可溶盐类皆被淋失,不发生盐演化现象,土壤只及于粘化作用,pH 值多属中性至微碱性。太行山麓的褐土因受石灰性沉积物的覆盖,发生次生碳酸盐化作用,土壤剖面中有假菌丝体存在。浅色草甸土多分布于冲积平原,其形成过程受地下水的影响极显著。地下水埋藏深度约2—3米,也可达4—5米。由于地下水升降频繁,氧化还原作用交替进行,土壤中呈现显明的锈纹斑,但无假菌丝体。土壤疏松多孔而有结构性,因土壤中有机质较少、土色浅淡而多受人为耕作的影响,故称耕种浅色草甸土。洼地及湖淀附近,地下水埋藏较浅或地表积水,土壤发生沼泽化过程。山麓交接洼地,积水时期长久,潜育作用及腐殖质积累均较显著。平原中洼地比较平坦,积水时间亦较短,腐殖质积累和潜育作用都较轻微。海滨洼地中,潜育作用较为剧烈,但有机质的积累则不一致,水浅处的有机质积累较多。因地形及地下水的情况不同,土壤盐渍程度各地不一。盐渍土多发生于山前交接洼地、碟形洼地边缘,以及槽状洼地和地上河流的两侧。有些灌区由于缺乏合理的灌排系统和灌溉制度,土壤发生了次生盐演化现象。华北平原盐渍土可分为内陆及海滨两种:内陆盐渍土多属氯化物硫酸盐土,地下水埋藏深度约1.5—2.0米,地下水矿化度约1—3克/升;海滨盐土区多属氧化物盐土,地下水埋藏深度约1.0—1.5米,地下水矿化度大于10克/升;过渡地带(即海滨盐土与内陆盐土的过渡地带)的盐渍土多属硫酸盐氯化物盐土,地下水埋藏深度约1.5米左右,地下水矿化度5—10克/升。华北平原中的四个主要成土过程是互相联系,而且有过渡阶段的。褐土和浅色草甸土的形成条件,主要在于排水情况和地下水位的不同。所以这两种土壤分布毗鄰而有互相过渡的发展情况。扇形地中下部,地面排水尚好而地下水埋藏较浅(1.5—3米),褐土区中可发育浅色草甸褐土。在泛盐平原中地势相对高起的黄河故道或靠近冲积扇地区,地下水埋藏较深(3.5—5米),可发育褐土化浅色草甸土。泛溘平原中的洼地积水愈久,沼浑化过程愈强,可由沼泽化浅色草甸土过渡至浅色草甸沼泽土或沼泽土。但经人工挖沟排水或洼地淤平以后,土壤可由沼泽土转向浅色草甸过程或褐土过程发展。浅色草甸土中如地下水埋藏浅而矿化度高,则土壤可向盐土方向发展。海滨盐土如不再受海潮影响和改善排水情况,则土壤也可由盐土向浅色草甸土发展。

Clay particles of less than 1μ were separated from 18 selected soil samples, representing important types of red and yellow soils of southern China.Com- position of clay minerals was identified by X-ray defraction,differential ther- mal analysis,base exchange capacity and chemical constituents.Zonality of the weathering stage of the soil,as shown in Fig.I,is explained briefly as follows. Region(Ⅰ)Lateritic soils Representative clay minerals:Kaolinite-gibbsite-hematite.Soils of this type mainly distribute on...

Clay particles of less than 1μ were separated from 18 selected soil samples, representing important types of red and yellow soils of southern China.Com- position of clay minerals was identified by X-ray defraction,differential ther- mal analysis,base exchange capacity and chemical constituents.Zonality of the weathering stage of the soil,as shown in Fig.I,is explained briefly as follows. Region(Ⅰ)Lateritic soils Representative clay minerals:Kaolinite-gibbsite-hematite.Soils of this type mainly distribute on the rolling hills of northern Hainan island,Laichou peninsula and south-central Yunnan.Formation of lateritic soil seems confined to the highly weathered parent materials of basalt origin,which were formed possibly at tertial geological age.Present direction of soil development remains much controversy. The whole soil contains around 20% Fe_2O_3 as hematite.Clay portions (<1μ)of the soil possess base exchange capacity 5—5.5 m.e.per 100 grams and SiO_2/Al_2O_3 ratio 1.4—1.5. TiO_2 in form of ilmenite presents both in silt and clay fractions up to 4—6%. Region(Ⅱ)Red soils of tropic zone Representative clay minerals:Kaolinite-halloysite.Soils of this type form a narrow belt in the tropic zone,extending from southern Fukien to Kwangsi. They are derived from various parent materials,including granite,metamor- phic rocks,sand stones,shales and marine deposits.Clay minerals of kaolinite group are the characteristic weathering product of this soil type with minor portions of gibbsite,hematite,quartz,and illite. Clay fractions of this soft type possess base exchange capacity 10—15 m.e. per 100 grams and SiO_3/Al_2O_3 ratio 1.7—2.0. Region(Ⅲ)Red soils of subtropic zone Representative clay minerals:Kaolinite-quartz-Montmorillonite.Soils of this type distribute in the subtropic zone of south-cntral China,occurring on the low hills and terraces below 500—600 meters altitude.They are derived from granite,phyllite,sandstones,shales and red clay.The much higher ex- change capacity of clay fraction(20—25 m.e.per 100 grams),higher SiO_2/Al_O_3 ratio(2.0—2.3),together with the identified clay minerals characterize the less advanced weathering stage in comparison to the soils of tropic zone. In the silt fraction of this soil type much of orthoclass and mica remain undecomposed. Region(Ⅳ)Yellow soils on the mountainous region of southern China Representative clay minerals.Kaolinite-montmorillonite,Illitequartz and montmorillonite-quartz. On the higher mountains above 600—700 meters altitude of southern China, including both tropic and subtropic zones,yellow soils and partially red soils occur.Clay minerals of this soil type characterize a moderately weathering stage.Montmorillonite,illite,kaolinite and quartz are the major constituents, but variations of the composition of these minerals are determined by the primary minerals of their parent rocks. Clay fractions of this soil type possess base exchange capacity 24—34 m.e. per 100 grams,with higher content of active alumina up to 2.5—5.5 m.e.per 100 grams. Soils occurring on the depression area of red earth region usually appear yellowish.The diversity of soil color leads much controversies in soil classifi- cation.Present investigation indicates that the change from reddish coloration to yellowish in the depression area is induced by the hydration of hematite. Once a small portion of the anhydrous ferric oxide has been hydrated into geothite or limonite due to local variation of the moisture condition,while the main constituents of the clay minerals remain unchanged,the soil gives a dis- tinctive yellowish coating.The change is very sensitive.

1.用 X-光分析,差热分析,化学分析和代换量测定方法,综合鉴定了华南砖红壤性红壤,热带红壤,亚热带红壤和山地黄壤的粘土矿物组成,并绘制了华南土壤主要粘土矿物组成分区图。我们将华南土壤分为四个区,即砖红壤性红壤区,主要粘土矿物为高岭石,三水铝石,赤铁矿;热带红壤区,主要粘土矿物为高岭石,埃洛石;亚热带红壤区以高岭石,石英,濛脱石为主;山地黄壤区,以伊利石,濛脱石,石英,高岭石为主,其组合因母岩的不同而转移。2.我们对微域地形,如坡上、坡下;南坡、北坡和局部气候的影响,使土壤颜色发生了显著的变化的红色,黄色土壤进行了研究。结果证明,二者的化学性质、粘土矿物组成完全相同。在低洼地区和阳坡等湿润条件下赤铁矿部分水化成为针铁矿,因之使土壤颜色变黄。但这种黄色土壤与风化程度较浅的山地黄壤是有很大区别的。3.我们把由浅海沉积物母岩发育,过去称为砖红壤性红黄色土的土壤,划归红壤。因为我们研究结果证明,这类土壤的风化程度并不比红壤深些,它们的粘士矿物组成和化学性质与热带地区的红壤也很一致。砖红壤性土壤,仅仅局限于一定的母岩。4.在紫红色砂岩发育的山地黄壤中发现了一水软铝石的存在,对它的生成、转变尚待进一步研究。

 
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