some t2 terrace soils of peninsular malaysia: i ... papers/pert vol. 6 (3) dec... · some t2...

Pertanika 6(3), 61-89 (1983)

Some T2 Terrace Soils of Peninsular Malaysia: I. Micromorphology,Genesis and Classification

J. SHAMSHUDDIN and E. TESSENSSoil Science Department, Faculty of Agriculture,

Universiti Pertanian Malaysia, Serdang, Selangor, Malaysia.

Key words: T2 terrace soils; Peninsular Malaysia, micromorphology; genesis; classification

RINGKASAN

18 profil yang terdiri daripada 14 siri tanah teres T2 di Semenanjung Malaysia telah dikaji. Tanah-tanah ini berasal daripada bahan aluvium campuran yang berumur Holosen. Kebanyakan tanah itu dikelas-kan sebagai Inseptisol Yang lain-lainnya pula dikelaskan sebagai En'tisol, Ultisol dan Alfisol Kajianini menunjukkan tanah-tanah tersebut berada sama ada di peringkat luluhawa baharu atau pertengahan.Taburan pertalian k/h ialah gefurik di dalam famili berpasir, gefurik dan/atau kitonik di dalam familiberlom kasart dan porpirik di dalam famili berlom halus dan berlempung. Adalah diketahui bahawa pitolislebih sering dijumpai di pantai timur daripada di pantai berat.

SUMMARY

18 profiles belonging to 14 soil series of the T2 terrace soils of Peninsular Malaysia were studied.The soils are derived from alluvial materials of mixed origin of Holocene age. They are mainly Inceptisols.Others are classified as Entisols, Ultisols and Alfisols. The study indicates that the soils are either in therecent or intermediate stage of weathering. The c/f related distribution is gefuric in the sandy families,gefuric and/or chitonic in the coarse loamy families, and porphyric in the fine loamy and the clayeyfamilies. It is found that phytoliths are more common in the east than in the west coast of the peninsula.

INTRODUCTION

About 40% of the land surface of PeninsularMalaysia is hilly or mountainous (Gopinanthanand Paramananthan, 1979). Most of the flat areasoccur in the alluvial plains, which are either marineor riverine in origin. Riverine alluvial depositsoccur at three levels, namely T3, T2 and Tj , whichare respectively referred to as high, intermediateand low terraces (Gopinanthan, 1968). Of parti-cular interest are the soils on T2 terraces becauseof their spatial distribution.

The objective of this study is to provideinformation for a complete taxonomic classifica-tion of T2 terrace soils as well as to study theirgenesis and micromorphology.

MATERIALS AND METHODS

18 pedons belonging to 14 soil series wereselected for the study. These are the soils ofNangka (1, 9), KampungPusu (2), Bukit Tuku (3),Kerayong (4, 12), Cherang Hangus (5), SungaiBuloh (7, 8, 13), Lintang (6), Subang (10), Sogo-mana(ll), Rasau (14), Napai(15), Chuping(17)

and Holyrood (18). The soils are named approxi-mating as much as possible the definition proposedby the Department of Agriculture (Paramananthan,1981).

The soils were sampled from many areas(Fig. 1), where T2 terrace soils are known to befound. These are around the vicinity of Pasir Mas,Kelantan (1, 2, 3, 4, 5), Kuala frengganu (6),Batu Pahat (8, 9), Sungai Buloh, Selangor'(7),Lower Perak (10, 11, 12, 13, 14), Pokok Sena,Kedah (15), Pauh, Perlis (16) and Langkawi (17,18).

Types of samples taken are: —

1. Bulk samples for routine, physico-chemicaland mineralogical analyses.

2. Undistrubed samples in a Kubiena box formicromorphological analyses.

3. Core samples for physical analyses.

Analytical procedures are as follows: granulo-metric analysis was carried out by successivesedimentation. pH was determined both in water

61

J. SHAMSHUDDIN AND E. TESSENS

Fig. 1. A map of Peninsular Malaysia showing theposition of sampling (dot denotes the areaof sampling and number denotes pedon).

and IN KC1 after 1 day of equilibration. CECwas determined in IN NH4OAc buffered at pH 7and in IN NH4C1 solution. KC1 acidity (Al + H)was determined by the method of Yuan (1959).Extractable acidity was estimated by KC1-TEAbuffered at pH 8.2. Organic carbon was deter-mined by the Walkley-Black Method (Allison,1965) and nitrogen was determined by the methodof Bremner (1965). Free iron oxide was estimatedby the dithionite citrate bicarbonate (DCB) me-thod of Mehra and Jackson (1960). Base satura-tion is the sum of bases expressed as % of CEC(NH40AC), while Al saturation is the Al expressedas % of Al plus bases. Micromorphological descrip-tion was done following the proposal of Stoops(1978). Analytical data are given in the Appendix.

RESULT AND DISCUSSIONS

1. General consideration

1.1 ClimatePeninsular Malaysia is characterised by high

rainfall and uniformly high temperature. Themoisture regime of the well drained areas is

either udic or perudic. The rainfall is relativelyhigher in the south than in the north of thepeninsula, and most of Johor has a perudic mois-ture regime. The northern states of Kedah andPerlis have an udic moisture regime, with spottedplaces approaching ustic. The slight variation inclimate may have some influence on the genesisof the soils.

Soil temperature can roughly be estimatedby adding 2.5° C to the air temperature (Tavernier— private communication). Using this assumption,it is found that the soil temperature (at 50 cmdepth) in the areas under study varies from 28° Cto 30° C. The temperature regime is isohyper-thermic throughout the country as MSTT-MWSTis less than 5°C (MSST = mean summer soiltemperature, MWST = mean winter soil tem-perature).

L2 GeologyThe most important rock type in the penin-

sula is granite, occupying about 50% of the landsurface (Yeh, 1968). Other rock types are lime-stone, sandstone, shale, schist and basic igneousrocks (Gobbett, 1972; Yin and Shu, 1973). Themain rivers controlling the drainage pattern of thepeninsula are the Sg. Pahang (420 km), Sg. Perak(350 km) and Sg. Kelantan (280 km). Over theyears, the mouth of the rivers have shifted accor-ding to the direction of the prevalent current.For instance, Sg. Kelantan has moved 35 kmtoward northwest of the former river (Tjia, 1970;Tjia, 1973).

1.3 Sea Level Changes and Terrace FormationEvidence for the change in sea level in the

Quaternary is abundant. The presence of wave-cutnotches (Hodgkin, 1970) and marine beachdeposits (Nossin, 1961; 1964) are evidence forQuaternary sea level change. Evidence of a lateQuaternary change in sea level is widespread in theIndonesia Archipelago in the form of raised coralreefs and raised beach terraces (Kaile, 1970).Even prograding streams have been interpretedby Tjia (1970) as evidence of the fall in sea level.

Biswas (1973) found some evidence ofchanges in sea level from punch cores off the eastcoast of Peninsular Malaysia. Lithologic changescombined with foraminiferal and spore-pollendata indicate shallowing of extensive areas of theSouth China Sea. From the available data so far,Tjia (1973) proposed that the highest sea levelin the Quaternary was about 30-50 m above andthe lowest 100 m below the present sea level.It is assumed that the Quaternary changes insea level are at the origin of the terrace formation.

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SOMET2 TERRACE SOILS OF PENINSULAR MALAYSIA - I

1.4 Characteristics of Young A lluviumThe deposits forming the T2 terraces are

unconsolidated deposits of sand and gravel withsome clay and peat. These deposits, which can beequated to Young Alluvium (Subrecent Alluvium),are of Holocene age (< 10,000 years). The YoungAlluvium is characterised by unweathered orslightly weathered clasts and soils developed fromit are commonly less than 2 m deep (Stauffer,1973). The Young Alluvium of the Kinta Valleycontains an abundant amount of sedimentarystructures of fluvial origin (Sivam, 1969). Sivam(1968) found the age of this deposit to be about3000 years.

2. Geographical DistributionPhysiographically, T2 terrace soils are found

mainly at 20—30 m elevation, in areas adjacentto coastal plains, concentrated along major rivers.Up to this moment, over 25 soil series have beendefined and characterised by the Departmentof Agriculture (Paramananthan, 1980; 1981).

A quick look at the literature indicates thatthe most common T2 terrace soils are apparentlySogomana, Nangka, Rasau, Holyrood, Lintang,Kerayong and Sungai Buloh Series, which arefound in the alluvial plains of Kelantan,Trengganu,Pahang and Perak (Leamy and Panton, 1965;

Law, 1968; Gopinathan, 1968). Soils of CherangHangus, Gong Chenak, Bukit Tuku and KampungPusu Series occur almost exclusively in KelantanPlains (Arnott, 1957; Law, 1968). Other soils suchas the soils of Chuping and Napai series are respec-tively found in Perlis and Kedah.

3. Characterisation of the soils (Table 1)

3.1 Nangka Series (1, 9)These soils are characterised in the field by a

loamy sand top soil underlain by sandy loam. Thestructures are weak, medium, subangular blockyand the consistence is friable.

The microstructure of this subsoil is cavitied,with channels and vughs as the main type of pores.The coarse materials are dominated by quartz.The fine materials, which are brown in colour,have undifferentiated b-fa brie (1) or dotted scallyb-fabric (9). The undifferentiated b-fabric is theresult of coating by gibbsite (Stopps, 1978). Thec/f related distribution is chitonic and/or gefuric.Cavitied microstructure shows that the drainageis very good.

Physico-chemical and micromorphologicalstudies, and field observations indicate that thesoil is Typic Dystropept (Table 2). According

TABLE 1Field characteristics of T2 terrace soils of Peninsular Malaysia

(+ colour and texture at 50 cm depth).

SERIES

Nangka (1)Kampung Pusu (2)Bukit Tuku (3)Kerayong (4)Cherang Hangus (5)Lintang (6)Sungai Buloh (7)Sungai Buloh (8)Nangka(9)Subang(lO)Sogomana (11)Kerayong (12)Sungai Buloh (13)Rasau (14)Napai (15)Chuping (16)A wang (17)Holyrood (18)

COLOUR+

10YR2.5YR2.5Y10YRN7/10YR10YR10YR10YRN7/N7/10YR10YR2.5Y5YR10YR10YR7.5YR

(6/4)(7/3)(6/4)(6/6)

(5/6)(5/4)(7/6)(6/4)

(5/4)(5/4)(8/3)(5/8)(6/6)(6/1)(6/5)

TEXTURE+

sandy loamclay loamclay loamclayclaysandy loamcoarse sandcoarse loamy sandcoarse loamy sandfine loamy sandsilty clay loamclay loamloamy coarse sandloamsandy clayclay loamsandy clay loamsandy clay loam

STRUCTURE

weakmoderatemoderatemoderatemoderateweakstructurelessweakmoderatestructurelessweakmoderateweakmoderateweakweakweakweak

CONSISTENCE

friablefirmfirmfirmplasticfriableloosefriablefriablefirmfirmfirmfriablefirmfirmfriablefirmfriable

DRAINAGE

well drainedpoorimperfectmoderatepoorwell drainedexce«=iveexcessivewell drainedpoorpoormoderateexcessivewell drainedwell drainedimperfectimperfectwell drained

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3.9 Sogomana Series (11)This soils is clayey. A lower clay content

in the surface horizon is compensated by a veryhigh silt content. Detailed investigation of thetextural profile suggests the presence of lithologicdiscontinuities throughout the profile.

The soil has a cavitied and fissured, and occa-sionally, irregular jointed microstructure at depth.The pores are mainly vughs. The coarse materialsare composed of quartz and muscovite, while thefine materials consist of dotted, yellowish grayclay materials. The b-fabric is dotted scally andvery broad and thin cross fibrous. The c/f relateddistribution is open porphyric.

Irregular soil nodules (2—3 mm 0), which arecomposed of small nodules (< 100 um) in diffe-rent stages of formation, are present in the B2i %.Yellowish brown ferriargillans, with strong,continuous orientation, are present in the pores.The presence of thin patchy cutans, which wereobserved in the field, are therefore confirmed. Thisis a clear indication of clay translocation in theprofile. Field observations and laboratory analysesshow that the soil is a Typic Tropaquult or GleyicGleysoL

3.10 Rasau Series (14)The soil is recognised in the field by its loamy

texture and pale colour at depth. The structuresare moderate, medium and fine subangular block;and the consistence is friable.

The microstructure is also cavitied. Channelis the main type of pore. In the coarse materials,quartz, zircon and tourmaline are present. Thefine materials consist of dusty grey clay, withundifferentiated b-fabric. The c/f related distribu-tion is gefuric to close porphyric. The soil can beclassified as Oxic Dystropept.

3.11 Napai Series (15)Soils of Napai Series are enveloped on re-

worked lateritic materials from shale. Petroplin-thite is present in the form of loose penetrableconcretions, usually at shallow depth. The struc-ture of the top soil is weak to moderate, medium,subangular blocky. Thin patchy cutans were seenin the field. The study shows that the soil is amember of coarse loamy over clayey-skeletal,kaolinitic, isohyperthermic Typic Paleudults.

3A2 Chuping Series (16)This soil is developed on reworked lateritic

materials, resting on limestone of Chuping Forma-tion. The top soil is a light yellowish brown sandy

loam overlying and brownish yellow sandy clayloam.

Thin patchy cutans characterise the B hori-zons. Distinct, brownish yellow mottles appearin the B21t • Petroplinthite sometimes appear atshallow depth. Base saturation is high, being 100%at depth. This soil is therefore classified as coarseloamy over fine loamy-skeletal, mixed, isohyper-thermic, Aquic Tropudalf or Gleyic Luvisol.

3.13 AwangSeries (17)This soil is derived from parent material

originated from tourmaline rich granite. The topsoil is a light gray coarse sand. This is underlainby a light brownish gray loamy sand. The colourbecomes lighter with depth. Yellowish brownmottles appear in B22 showing that the drainageconditions are somewhat impeded. This soil can beclassified as Aquic-Oxic Dystropept. A thin sectionfor this soil is not available.

3.14 Holy rood Series (18)Thin continuous cutans characterise the B2

horizon. The top soil is brown sandy clay loam,overlying a light brown sandy clay loam. Thecolour becomes redder with depth, due to theincrease of Fe oxides with depth. On availabledata, this soil can be classified as Typic Paleudult.A thin section for this soil is not available. Thus itis not possible to prove the presence of cutansmicromorphologically. There is an increase of claycontent with depth. The presence of cutans andthe increase of clay with depth seems to indicatethat the soil is a Paleudult.

4. Genesis of T2 Terrace Soils

4.1 Influence of Soil Forming FactorsIt is apparent that the most important factors

affecting the soil forming processes of T2 terracesoils are parent material and climate. It is knownthat the most important rock unit in the countryis granite, occupying about 50% of the total landsurface (Yeh, 1968). These granite bodies formmountain ranges in the central and the eastern partof the peninsula.

The chief rivers, which control the drainagepattern of the peninsula, originate and draw theirwater from those mountains. On their way to thesea, the rivers cut through other rock types andcarry along with them deposits of varying com-position. The nature of the deposits vary fromclayey and silty to sandy materials. There isevidence to suggest that the textural and themineralogical composition of the alluvial depositsare, for an important part, influenced by thegranite mineralogy. The dominance of subangular

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SOME T2 TERRACE SOILS OF PENINSULAR MALAYSIA - I

tourmaline in the heavy mineral fraction of theVFS (Pettijohn, 1957) further justifies the abovestatement.

However, some of the soils on T2 terraceare silty and clayey. These sediments are probablynot derived solely from granite. THere are twopossibilities with regard to the origin of the parentmaterials of these silty clayey soils:

1. The parent material is originated fromshale, phyllite, schist or other fine grainedsedimentary or metamorphic rock.

2. The parent materials are deposited in a lowenergy environment, characterised by finesediments (Reineck and Singh, 1973).

The mouths of rivers in Peninsular Malaysiashift according to the direction of the prevalentlong shore currents. The rivers in Kelantan andTrengganu move northwards, while the rivers inKedah and Perlis move southwards (Tjia, 1973).The change in the course of these rivers maychange the composition of the deposits of the areabecause it influences the environment of deposi-tion. This may be at the origin of lithologicdiscontinuities and stratification of the sediments(see 5.1).

Coupled with parent material, climate andtime control the type and stage of weathering.Physico-chemical weathering of the deposits takesplace immediately after they are exposed to theatmosphere. With an annual rainfall exceeding2,000 mm in most parts of the country and amean annual temperature of about 27° C (Dale,1963), chemical weathering is intensive.

Topography and vegetation are playing amodifying role in this process of ferrallitic wea-thering. In the well drained areas, with importantremoval of silica and bases, weatherable mineralsare being transformed into kaolinite and/orsesquioxides, and in some cases, the soils arepractically devoid of weatherable minerals. On theother hand, where the drainage is impeded, feld-spar, muscovite and even biotite survive secondarytransformation. The best example of the latter isthe Subang Series (10).

42 FerrallitizationFerralitization is the chief soil forming process

in the humid tropics (Sys, 1979). This process ischaracterized by the dominance of 1:1 claymineral and/or sesquioxides, particularly gibbsite.As evidenced byXRD and thermal analyses (Sham-shuddin and Tessens, unpublished the studiedsoils have those minerals in the clay fraction.

Leaching and ^subsequently weathering issomewhat related fo the textural compositionof the original alluvial deposits. Thus in sandymaterials, leaching and weathering are so intensethat primary minerals or even kaolinite maytransform to gibbsite. Such transformation 4snoted in the soils of the Sungai Buloh Series (7),where gibbsite exceeds kaolinite in the clayfraction. On the contrary, in the loamy and theclayey materials, where leaching and weatheringare expected to be less intense, kaolinite do-minates over gibbsite.

4.3 Clay TranslocationIn most cases, cutans were not seen in the thin

sections. The ones which contain cutans can notbe considered as having argillic horizons as the% of cutans is less than 1%. As such, it is con-sidered that no major translocation of clay hasoccurred yet. In general, the soils contain a cambichorizon.

4A Weathering StageWeathering stage of soils can be defined by

various criteria. Among the criteria used are thesilt/clay ratio (Van Wambeke, 1962) and minera-logy of the clay fraction (Jackson and Sherman,1953). Stage of weathering can also be definedby the proposal of Sys (1979) or by the chargecharacteristics of the soils (Tessens and Sham-shuddin, 1982).

In spite of the limitation, due to the problemof changing lithology, silt/clay ratio can be usedsuccessfully to obtain the stage of weatheringof the studied soils, as follows: —

1. Recent stage — silt/clay ratio is more than1.

2. Intermediate stage — silt/clay ratio is1-0.2.

3. Advanced stage - silt/clay ratio is lessthan 0.2.

The studied soils can be grouped accordingly(Table 3).

It is seen that most of the soils are either inthe recent or in the intermediate stage of wea-thering. The soils of Subang Series (10) give thehighest value (3.68), implying that they are theleast weathered soils. Thin-section study indicatedthat the soil contains feldspar, muscovite andbiotite, consistent with the high silt/clay ratio.On the other hand, the most weathered of the soilsare the Napai (15) and the Holyrood Series (18);these soils are Paleudults.

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TABLE 3Stage of weathering of T2 terrace soils

according to silt/clay ratio

TABLE 4Stages of ferrallitic weathering

RECENT INTERMEDIATE

Nangka (1)

Bt. Tuku(3)

Subang(lO)

Sogomana(ll)

Kerayong(12)

Rasau (14)

Kg. Pusu (2)

Keryong (4)

Chg. Hangus(5)

Chuping(16)

Awang (17)

Lintang (6)

Nangka (9)

Napai (15)

Holyrood(18)

Feldspar and biotite are minerals in the recentstage of weathering (Jackson and Sherman 1953).Muscovite, vermiculite and montmorillonite areminerals in the intermediate stage while kaoliniteand sesquioxides are minerals in the advancedstage of weathering. Based on this consideration,it is found that the soils of Subang (10) andAwang Series (17) fall under recent stage ofweathering; these soils contain biotite and feld-spar. Soils in the intermediate stage of weatheringare the Nangka (1), Kampung Pusu (2), BukitTuku (3), Kerayong (4, 12), Cherang Hangus (15),Sogomana (11), Napai (15), Chuping (16) andHolyrood Series (18). Soils of Lintang (6) andSungai Buloh Series (7, 8, 13) seem to fit into theadvanced stage of weathering.

According to the stages of ferrallitic weatheringof Sys (1979), soils of Subang (10) and AwangSeries (17), which contain weatherable minerals,are in the recent stage (Table 4). Soils of SungaiBuloh Series (7, 8, 13) are difficult to put into thesystem, as they have no pedogenic developmentand dominated by kaolinite and/or gibbsite.Taxonomically, they are classified as Entisols.In this study, the soils are included in the recentstage of ferrallitic weathering. Other soils, withcambic or argillic horizons, are included in theintermediary stage.

In all systems, it is supposed that the soilchanges its properties on changing from recent toan advanced stage of weathering. This has adirect effect on the mineralogy and chemistryof the soil.

5. GENERAL DISCUSSION

5.1 Lithologic DiscontinuitiesIn the Kerayong Series (4), there appears to

be an increase of clay in the B2 ; the increase of

RECENT INTERMEDIARY

Sungai Buloh (7,8,13)

Subang (10)

Awang (17)

Nangka (1,9)

Kampung Pusu (2)

Bukit Tuku (3)

Kerayong (4)

Cherang Hangus (5)

Lintang (6)

Sogomana (11)

Rasau (14)

Napai (15)

Chuping (16)

Holyrood (18)

clay from A p is 6.3%. This definitely does notmeet the requirement of an argillic horizon. Anargillic horizon needs at least an increase of 8%for this clayey soil (USDA, 1975). The texturaldifferentiation in the profile then is rather due toa change in the environment of sedimentation.This is expressed in the VFS/sand %. A change ofVFS/sand % from 34.6% over 50.4% to 68.2%(Ap , B2i and B22 resp.) is an indication of thepresence of several lithologic discontinuitiesthroughout the profile.

Similarly, the VFS/sand % can be used toconfirm the presence of lithologic discontinuitiesin the soils of Cherang Hangus (5), Subang (10),Sogomana (11), Kerayong (15) and Awang Series(17). Such discontinuities were not recognizedin the field.

5.2 Micromorphology

5.2.1 Microstructure

It is noted for the soils in the sandy andcoarse loamy family that the microstructure iscavitied. This is well illustrated by the soils ofSungai Buloh (8, 13), Lintang (6) and NangkaSeries (1, 9). Likewise, the fine loamy family has acavitied microstructure. Cavitied and occasionallyfissured microstructures are found in the clayeysoils. Such is the case for the soils of KampungPusu (2), Kerayong (4, 12), Cherang Hangus (5)and Sogomana Series (11).

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Microstructure is related to the porosity ofthe soil. Cavitied microstructure is usually asso-ciated with high porosity, meaning that watercan pass through easily.

5.2.2 Coarse Materials (> 10 urn)

Regardless of texture, the most commonmineral in the coarse materials, in these soils,is quartz. These quartz grains vary in size fromcoarse to fine, with a subangular to angular shape.Roundness of the grains will, to a certain extent,provide information on the distance of transporta-tion before final deposition takes place, as grainswhich have undergone a long distance of transpor-tation are usually rounded.

Other minerals in the coarse materials arezircon and tourmaline. According to Pettijohn(1957), rounded tournaline and zircon originatefrom reworked sediments, while euhedral tourma-line and zircon originate from acid igneous rock.Most of the tourmaline and zircon in the studiedsoils are subangular in shape. This is an indicationthat the soil material is influenced by acid igneousrocks, transported over some distance.

5.2.3 Fine materials (< 10 urn)

The fine materials consist of clay minerals,varying in colour from grey to red. From themineralogical studies, it is found that these ma-terials are mainly kaolinite, 2:1 minerals andmixed layers. Beside these, there is also an impor-tant amount of gibbsite, especially in the sandysoils. The gibbsite coatings affect the b-fabric ofthe fine materials.

The undifferentiated b-fabric seen in thesandy soils is probably the result of gibbsitecoating and/or masking of this sesquioxidicmaterials on the clay surfaces (Stoops, 1978;Eswaran et alf 1979). Under crossed polarizers,the fine materials are almost isotropic. Theb-fabric of the clayey soils is either scally orfibrous or both. This type of b-fabric is present inthe soils of Kampung Pusu (2), Kerayong (4)Cherang Hangus (5) and Sogomana Series (11).

5.2.4 C/F Related Distribution

The c/f related distribution of T2 terracesoils depends for an important part on the texturalcomposition of the soils. In the sandy family,the c/f related distribution are locally observedin these soils. This type of c/f related distributionis noted for the soils of Sungai Buloh Series (8, 13).

As the amount of clay in the soils increases,the c/f related distribution tends toward porphyric.

In the coarse loamy family, such as Nangka (1)and Lintang (6), the c/f related distribution isgefuric and/or chitonic, tending toward porphyric.Soils of Bukit Tuku (3) and Rasau Series (14),which are fine loamy, have porphyric c/f relateddistribution. Gefuric c/f related distribution wasfound only occasionally in these soils. The c/frelated distribution of the clayey soils, such as theKampung Pusu (2), Kerayong (4, 12), CherangHangus (5) and Sogomana Series (11), is almostexclusively porphyric. Texture plays an importantrole in the formation of the name c/f relateddistribution. It is the clays that bind togetherand coat the coarse materials.

Related to classification, gefuric is commonin Entisols. Among the gefuric, chitonic, enaulicand porphyric, the more developed profiles haveat least two of these c/f types.

5.2.5 day Cutans

The consequence of physical translocation ofclay mineral in the soil is the formation of anargillic horizon. One of the conditions for theformation of this horizon is minimal soil pedotur-bation, in order to prevent the assimilation ofthe argillans into the matrix (Eswaran et al,1979). Formation of the argillans is a dispersion-

deposition phenomenon (Eswaran and Sys, 1979).The subject of clay cutans is an important issuein this study, as clay cutans are an importantparameter in soil classification.

In the field, all the clayey soils and some ofthe loamy soils were described as having thinpatchy cutans. When these soils were examinedunder the microscope, clay cutans could not beidentified, except occasionally in the soils of BukitTuku (3) and Lintang Series (6); only the soilsof Sogomana Series (11) contain a sufficientamount of cutans. The soils of Kampung Pusu (2),Kerayong (4, 12) Cherang Hangus (5) and RasauSeries (14) do not show the presence of claycutans. *

The problem of cutans identification has alsobeen discussed at length by Beinroth (1982)for soils of Puerto Rico. It was found that fieldobservation of clay skins and their distinctionfrom stress cutans is a serious difficulty in soilshaving clayey texture and kaolinitic mineralogy.For instance, an Oxic Tropohumult, which hasbeen described as having many clay skins in thefield, was found to contain only 2% cutans. On theother hand, another soil, which had been classifiedas Oxisol, contained 4% cutans. '"he unequivocalrecognition of an argillic horizon as defined in

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Soil Taxonomy poses serious problems in the soilsof the humid tropics.

5.2.6 PhytolithsThese are opaline silica and therefore are

isotopic under crossed polarizers. Under polarizedlight, phytoliths have characteristics of rectangularplant cells, with a rather high negative relief(Stoops, 1978). The XRD pattern resembles thatof high temperature silica (crystobalite), with astrong reflection peak at 4A (Brown et al, 1.978).This peak was seen many times in the XRDdiffractograms of the silt fraction. The soils thatcontain phytoliths are Lintang (6), Kerayong (4),Cherang Hangus (5) and Bukit Tuku Series (3). Allof these soils are from the east coast of PeninsularMalaysia. Soils on T2 terrace from the west coastappear to contain few or no phytoliths, as evi-denced from the study of thin-sections.

CONCLUSION

Some T2 terrace soils are found in PeninsularMalaysia. These soils are either in a recent orintermediate stage of weathering, shown by thesilt/clay ratio and mineralogy. Most of the soilscontain some cutans, but could not be regardedas illuviation cutans as the amount is less than 1%required for an argillic horizon. These soils aretherefore classified as Inceptisols. The sandy soilslack pedogenic development and are classifiedas Entisols. Others are either Ultisols or Alfisols.

The change of clay content with depth is dueto a change in the environment of sedimentationrather than clay illuviation. The presence oflithologic discontinuities in the profiles is shownby a change of the VFS/sand % ratio. The c/frelated distribution of sandy soils is gefuric,while those of coarse loamy is gefuric and/orchitonic. The fine loamy and clayey soils haveporphyric c/f related distribution. Phytoliths aremore common in the east than the west coast ofthe peninsula.

ACKNOWLEDGEMENT

The authors wish to record their gratitude toProf. C. Sys and Prof. G. Stoops of the StateUniversity of Ghent for supervising the research,and UPM and ABOS for financial support. Theyalso wish to thank Dr. Paramananthan for hishelp in the sampling.

REFERENCES

ALLISON, LE. (1965): Organic carbon by Waikley-Black Method. In: "Methods of Soil Analysis".Black, C.A. (Ed.). Agronomy Monograph. 9: 1367-1378.

ARNOTT, G.W. (1957): The Kelantan deficiency area.Malays. Agric. J. 40: 60-91.

BEINROTH, F.H. (1982): Some highly weathered soilsof Puerto Rico, 1. Morphology, formation andclassification. Geoderma. 27: 1—73.

BISWAS, B. 1973): Quaternary changes in sea level inSouth China Sea. Bull Geol Soc. Malays. 6: 229-256.

BREMNER, J.M. (1965): Total nitrogen. In: "Methodsof Soil Analysis". Black, C.A. (Ed.). AgronomyMonograph. 9: 1149-1178.

BROWN, G., NEWMAN, A.C.D., RAYNER, J.H. andWEIR, A.H. (1978): The structure and chemistry ofSoil Constituents". Greenland, D.J. and Hayes,M.H.B. (Eds.). New York. John Wiley and Sons.29-78.

DALE, W.L. (1983): Surface temperature of Malaya./ Trop. Geog. 17:57-73.

ESWARAN, H. and SYS, C. (1979): Argillic horizon inLAC soils: formation and significance to classifica-tioa Pedologie. 2(2): 175-190.

ESWARAN, H. VAN WAMBEKE, A. and BEINROTH,F.K (1979): A study of some highly weathered soilsof Puerto Rico: Micromorphological properties.Pedologie. 29(2): 139-162.

FAO/UNESCO (1974): Soil Map of the World. Vol. 1.Legend. UNESCO, Paris.

GOBBETT, D.J. (1972): Geological Map of the MalayPeninsula, Geol Soc. Malays., Kuala Lumpur.

GOPINATHAN, B. (1968): Terrace and alluvial soils inWest Malaysia. Proc. 3rd Malaysian Soil Conference.Malaya. Soc. Soil Set, Sarawak, pp. 45-50.

GOPINATHAN, B. and PARAMANANTHAN, S. (1979):Steepland soils in Peninsular Malaysia. Proc. Malay-sian Seminar on Fertility and Management of De-forested Soils. Soc. Agric, Set Sabah and Malays.Soc. Soil Set, pp. 61-68.

HAILE, N.S. (1970): Radiocarbon dates of Holoceneemergence and submergence in Tembelau andBunguraxi Islands, Sunda Shelf, Indonesia. Bull.Geol Soc. Malays 3: 135-137.

HODGKIN, E.P. (1970): Geomorphology and biologicalerosion of limestone coast in Malaysia. Bull GeolSoc. Malays. 3: 27-51.

JACKSON, M.L. and SHERMAN, G.D. (1953): Chemicalweathering of mineral soils. Adv. in Agron. 5:219-318.

LAW, W.M. (1968): Reconnaissance Soil Map of Penin-sular Malaysia. Ministry of Agriculture and Coopera-tive, Kuala Lumpur.

LEAMY, M.L and PANTON, W.P. (1965): A Soil SurveyManual For Malayan Conditions. Soil ScienceDivision, Ministry of Agriculture and Cooperative,Kuala Lumpur.

MEHRA, O.P. and JACKSON, M.L. (1960): Iron oxideremoval from soils and clays by dithionite-citrate

70

SOMET2 TERRACE SOILS OF PENINSULAR MALAYSIA - I

system with sodium bicarbonate buffer. Clays andClay Minerals. 7: 317-327.

NOSSIN, J.J. (1961): Relief and coastal developmentin north-eastern Johore. J. Trop. Geog. 15: 27-39.

NOSSIN, J.J. (1964): Beach ridges in the east coast ofMalaya./ Trop, Geog. 18: 111-117.

PARAMANANTHAN, S. (1980): Draft field legend forsoil survey in Peninsular Malaysia. Soil ScienceDivision, Ministry of Agriculture and Rural Develop-ment, Kuala Lumpur.

PARAMANANTHAN, S. (1981): Simplified key to theidentification of Peninsular Malaysia (In press).

PETTIJOHN, F.J. (1957): Sedimentary Rocks. NewYork. Harper and Row Publication.

REINECK, H. and SINGH, I.B. (1973): Depositionalsedimentary Environments. New York. Springer-Verlag.

SlVAM, S.P. (1968): Radiocarbon dates in Kinta Valley.Newsletter. Geol Soc. Malays. 15(1).

SlVAM, S.P. (1969): Quaternary alluvial deposits inNorth Kinta Valley, Perak. M.Sc. thesis, U.M.,Kuala Lumpur.

STAUFFER, P.H. (1973): Cenozoic. In "Geology of theMalay Peninsular". Gobbett, D.J. and Hutchison, C.S.(Ed.). New York. John Wiley and Sons. pp. 143-176.

STOOPS, G. (1978): Provisional notes on micropedology.ITC, Rug., Belgium.

SYS, C. (1979): Tropical soils. II. ITC, Rug., Belgium.

TESSENS, E. and SHAMSHUDDIN, J. (1982): Charac-teristics related to charges in Oxisols of PeninsularMalaysia. Pedologie 32: 85-106.

TJIA, H.D. (1970): Monsoon-control of the easternshorelines of Malaya. Bull Geol Soc Malays. 3:9-15.

TJIA, H.D. (1973): Geomorphology. In: Geology of theMalay Peninsula. Gobbett, D.J. and Hutchison, C.S.(Eds.). New York. John Wiley and Sons. pp. 13-24.

USDA (1975): Soil Taxonomy: A basic system of soilclassification for making and interpreting soil survey.USDA Handbook No. 436. Washington.

VAN WAMBEKE, A. (1962): Criteria for classifyingtropical soils by age. J. Soil Set 13: 124-132.

YEH, C.S.K. (1968): Regional geology: West Malaysia.Brief outline of the geology of West Malaysia.Malays. Geol Surv. Rept pp. 53-67.

YIN, E.H. and SHU, Y.K. (1973): Geological Map ofPeninsular Malaysia. Geological Survey Malaysia.Ipoh.

YUAN, T.L. (1959): Determination of exchangeablehydrogen by titration method. Soil Set 88: 164-167.

(Received 25 February 1983)

71

PROFILE 1:

Hor

Ap

fefl

Hor

Ap

B2i

B22

Hor

A

B22

B22

NANGKA SERIES

Depth(cm)

0-25

25-69

69-125

pH(l

H2O

5.7

6.0

5.3

Na

0.08

tr

0.04

J. SHAMSHUDDIN AND E.

APPENDIX

Fine Earth (%)

Clay

8.50

9.20

12.1

:1)

KC1

4.4

4.2

4.2

Silt

8.50

12.8

10.5

Sand

83.0

78.0

77.4

Ext. A Exch. A

meq/100 q i

4.70

2.88

2.66

Bases

K Mg

meq/lOOgsoil

0.06

0.02

0.02

0.17

0.11

0.08

0.48

0.24

0.90

Ca

2.36

1.41

2.71

Particle Size

VFS

4.73

4.60

4.78

Al

foil

0.43

0.14

0.90

£ Bases

2.67

1.54

2.85

TESSENS

Analysis

Sand (%)

FS

28.3

23.6

23.6

Al.S

%

14

8

24

B.S

%

48

43

98

MS CS

27.5 13.9

27.8 15.7

27.1 15.2

Fe2O3 O.C

% %

0.21 1.27

0.29 0.24

0.29 0.12

CEC

NH4OAC

VCS

8.32

6.20

6.44

N

%

0.09

0.05

0.02

NH4CI

meq/100 g soil

5.60

3.60

2.90

2.90

1.80

1.60

VFS%

Sand

5.70

5.23

6.18

C/N

14.1

4.8

6.0

App.CECmeq/

100 g

65.9

39.1

23.9

72


PROFILE 2: KG PUSU SERIES

Hor

Ap

B2i

B22

Hor

Ap

B21

B22

Hor

Ap

B22

Depth(cm)

0-21

21-46

46-100

pH (1 :

H2O

4.9

5.0

5.1

Na

0.04

tr

0.04

Clay

35.4

37.9

29.4

1)

KC1

4.0

3.8

3.8

K

Fine Earth (%)Silt Sand

25.3

21.6

20.3

39.3

40.5

50.3

Ext. A Exch. A

meq/lOOq

23.7

18.0

12.8

Bases

Mg

meq/lOOgsoil

0.12

0.02

0.02

0.32

0.09

0.09

3.52

2.96

2.72

Ca

0.57

0.40

0.38

Particle Size Analysis

VFS FS

10.8

11.4

14.2

Al

soil

3.21

2.85

2.49

2 Bases

1.05

0.51

0.53

19.3

18.8

24.2

ALS

%

75

85

82

B.S

%

6

4

4

Sand (%)MS CS

5.70 2.89

6.54 2.93

7.40 3.14

Fe 2 O 3 O.C

% %

0.84 5.31

0.97 0.18

0.21 0.03

CEC

NH4OAC

meq/100 %

18.1

11.5

12.2

vcs

0.59

0,74

1.38

N

%

0.16

0.05

0.05

NH4CI

; soil

6.60

4.80

5.40

VFS%

Sand

27.5

28.1

28.2

C/N

33.2

3.6

0.6

App.CECmeq/

100 g

51.1

30.3

41.5

73


PROFILE 3: BT TUKU SERIES

Hor

Ap

B21

Hor

Ap

B21

Depth(cm)

0-16

16-58

58-130

pH(l

H2O

4.8

5.0

5.0

Fine Earth (%)Clay Silt Sand

17.9

28.7

31.5

: l )

KC1

3.7

3.8

3.7

41.9

39.1

36.3

Ext. A

40.2

32.2

32.2

Exch. A

meq/100 q

16.7

19.2

12.8

2.32

2.88

3.92

Particle

VFS

17.0

15.3

14.8

Al

soil

2.14

2.60

3.60

Size Analysis

FS

19.9

14.7

15.2

Al.S

%

74

84

88

Sand (%)MS

2.60

1.86

1.63

Fe2O3

%

0.36

1.14

1.04

CS

0.61

0.23

0.44

O.C

%

0.81

0.08

0.06

VCS

0.09

0.05

0.18

N

%

0.09

0.05

0.05

VFS%

Sand

42.3

47.5

46.0

C/N

9.0

1.8

1.2

2 Bases B.S CEC App.CEC

Hor Na K Mg Ca % NH4OAC NH4C1 meq/

meq/100 g soil meq/100 g soil 100 g

Ap 0.04 0.08 0.22 0.43 0.77 5 14.3 2.70 79.9

B21 0.04 0.02 0.08 0.36 0.50 5 10.9 4.80 38.0

11.2 6.20 35.6

0.04

0.04

tr

0.08

0.02

0.02

0.22

0.08

0.10

0.43

0.36

0.37

0.77

0.50

0.49

5

5

4

74


PROFILE 4: KERAYONG SERIES

Hor

Ap

B21

B22

Hor

Ap

B 2 i

B22

Hor

Ap

B21

B22

Depth(cm)

0-28

28-64

64-125

PH(1

H2O

5.9

5.0

5.2

Na

0.12

tr

to

Clay

53.5

59.8

54.4

: 1)

KC1

4.4

3.9

3.8

K

Fine Earth (%)

Silt

38.1

32.1

43.9

Sand

8.40

8.10

1.70

Ext, A Exch. A

meq/100 q

17.6

17.6

11.2

Bases

Mg

meq/100 g soil

0.17

0.21

0.05

3.06

0.16

0.28

0.40

4.24

5.20

Ca

2,98

0.40

0.35


VFS

2.91

4.08

1.16

Al

soil

0.11

3.85

4.21

£ Bases

6.33

0.80

0.68

FS

4.04

3.82

0.39

Al.S

%

2

83

86

B.S

%

39

8

6

Sand (%)

MS CS

0.57 0.37

0.16 0.04

0.09 0.04

Fe2O3 O.C

% %

1.77 1.74

2.29 0.24

2.29 0.09

CEC

NH4OAC

meq/100 g

16.2

10.1

11.2

vcs

0.50

0

0

N

%

0.05

0.04

0.04

NH4CI

; soil

9.60

10.1

11.0

VFS%

Sand

34.6

50.4

68.2

C/N

34.8

6.0

2.3

App.CECmeq/

100 g

30.3

16.9

20.6

75


PROFILE 5: CHG HANGUS SERIES

Hor

Ap

B21

B B

Hor

Ap

B2i

B22

Hor

Ap

B2i

Bn

Depth(cm)

0-20

20-54

54-90

pH(l

H2O

4,7

5.1

5.3

Na

0.04

0.04

0.04

Clay

64.1

53.1

43.2

:1)

KC1

3.7

3.7

3.9

K

Fine Earth (%)

Silt

34.3

44.2

47.3

Sand

1.60

2.70

9.50

Ext. A Exch. A

meq/lOOq

22.8

11.4

9.74

Bases

Mg

meq/100 g soil

0.08

0.05

0.07

0.24

4.44

6.02

5.84

4,00

2.88

Ca

0.51

0.74

0.91

Particle Size

VFS

1.02

2.23

7.03

Al

soil

4.53

3.21

2.67

£ Bases

0.87

6.26

7.04

Analysis

FS

0.31

0.32

0.86

Al.S

%

84

38

27

B.S

%

5

35

49

Sand (%)

MS

0.12

0.09

0.20

F e 2 O 3

%

1.J5

4.72

4.72

CS

0.04

0.05

0.16

O.C

%

0.51

0.18

0.09

CEC

NH4OAC

vcs

0.05

0

0.82

N

%

0.06

0.02

0.04

NH4CI

meq/100 g soil

17.9

15.2

14.4

14.4

13.2

12.0

VFS%

Sand

63.8

82.6

74.0

C/N

8.5

9.0

2.3

App.CECmeq/

100 g

27.9

28.6

33.3

76


PROFILE 6: LINTANG SERIES

Hor

Ap

Bi

B21

B22

B23

Hor

Ap

Bi

B2!

B22

B23

Depth(cm)

0-25

25-37

37-65

65-105

105-115

pH(l

H2O

5.1

4.7

4.8

4.9

4.7

Clay

14.9

13.8

15.9

19.9

23.1

:1)

KC1

3.8

3.8

3.8

3.9

3.9

Fine Earth (%)

Silt

5.81

4.77

4.06

4.78

3.87

Sand

79.3

81.4

80.0

75.3

73.0

Ext. A Exch. A

meq/lOOq

8.80

6.40

7.16

0.60

4.04

1.52

1.60

1.68

1.04

1.28


VFS

2.65

2.42

1.86

2.63

3.13

Al

soil

0.58

0.78

0.81

0.36

0.55

FS

17.6

10.4

7.68

13.3

12.3

Al.S

%

62

79

61

71

71

Sand (%)

MS

16.9

17.0

14.8

18.1

16,5

F e 2 O 3

%

0.57

0.93

0.57

0.93

0.93

CS

21.2

29.2

29.2

28.9

25.1

O.C

%

0.85

0.22

0.28

0.19

0.19

vcs

21.0

22.4

26.1

14.3

15.9

N

%

0.07

0.04

0.06

0.03

0.04

VFS%

Sand

3.34

2.97

2.33

3.49

4.29

C/N

12.1

5.5

4.7

6.3

4.8

Bases £ Bases B.S CEC App.CEC

Hor Na K Mg Ca % NH4OAC NH4C1 meq/

meq/100 g soil meq/100 g soil 100 g

Ap tr 0.08 0.18 0.10 0.36 7 5.40

Bi tr 0.03 0.08 0.10 0.21 6 3.80

B21 tr 0.06 0.07 0.38 0.51 13 4.00

B22 tr tr 0.05 0.10 0.15 4 3.40

B23 tr 0.01 0.04 0.18 0.23 7 3.40

3.00

2.40

2.60

2.80

3.00

36.2

27.5

25.2

17.1

14,7

77


PROFILE 7: SG BULOH SERIES

Hor

Ap

ACi

AC2

C

Hor

Ap

A d

AC2

C

Hor

Ap

AC

AC2

C

Depth(cm)

0-43

43-77

77-107

107-150

pH(l

H2O

4.4

4.7

4.9

5.4

Na

tr

tx

tr

tr

Clay

2.20

3.80

3.37

0.71

:1)

KC1

4.2

4.6

4.6

5.1

K

Fine Earth (

Silt

3.77

5.03

4.41

4.48

%)Sand

94.0

91.2

92.2

94.8

Particle Size

VFS

5.25

6.55

7.28

9.10

Ext. A Exch. A Al

meq/100 q soil

3.06

1.32

0.76

0.44

Bases

Mg

meq/100 g soil

tr

tr

tr

tr

0.10

0.08

0.02

0.03*

0.64

0.32

0.32

0.08

Ca

0.52

0.24

0.23

0.29

0.55

0.15

0.06

0.08

l Bases

0.62

0.32

0.25

0.32

Analysis

FS

18.0

20.3

23.2

23.5

Al.S

%

47

32

19

20

B.S

%

21

23

25

53

Sand (%)

MS CS

20.6 30.8

20.5 30.7

19.1 25.6

19.1 27.2

Fe2O3 O.C

% %

0.51 0.97

0.70 0.22

0.70 0.18

0.33 0.05

CEC

NH4OAC

vcs

19.4

13.1

17.4

16.5

N

%

0.07

0.01

0.01

0.01

NH4C1

meq/100 g soil

3.00

1.40

1.00

0.60

0.60

0.40

tr

tr

VFS%

Sand

5.59

7.18

7.90

9.60

C/N

13.9

22.0

18.0

5.0

App.CECmeq/

100 g

136.4

36.8

29.7

84.5

78



Hor

Ap

AC,

AC2

AC3

Hor

Ap

Ad

AC2

AC3

Depth(cm)

0-24

24-65

65-106

106-115

pH(l

H2O

4.5

4.8

4.8

4.8

Clay

5.94

8.36

8.74

0.26

:1)

KC1

3.7

3.9

3.8

3.8

Fine Earth (%)

Silt

6.65

4.51

4.93

4.02

Sand

87.4

87.1

86.3

86.7

E x t A Exch. A

meq/100 q

4.38

1.76

1.86

1.84

1.12

0.80

0.80

1.04


VFS

4.03

3.39

3.30

2.98

Al

soil

1.08

0.68

0.58

0.71

FS

17.1

14.2

13.8

12.0

Al.S

%

60

63

55

56

Sand (%)

MS

23.2

19.6

21.0

20.6

Fe2O3

%

0.52

0.43

0.52

0.52

cs

30.8

34.2

31.5

33.0

o.c

%

1.64

0.18

0.09

0.08

vcs

12.3

15.6

16.6

18,0

N

%

0.04

0.01

0.01

0.01

VFS%

Sand

4.61

3.89

3.82

3.44

C/N

41.0

18.0

9.0

8.0

Bases 2 Bases B.S

Hor

Ap

AC,

AC2

AC3

Na

tr

tr

tr

tr

K Mg

meq/100 g soil

tr

tr

tr

tr

0.08

0.04

0.05

0.04

Ca

0.64

0.36

0.42

0.51

0.72

0.40

0.47

0.55

%

15

25

34

46

CEC

NH4OACmeq/100 g

4.80

1.60

1.40

1.20

NH4CI

soil

1.60

0.60

0.80

0.80

App.CECmeq/100 g

80.8

19.1

16.0

i3.0

79


PROFILE 11: SOGOMANA SERIES

Hor

Ap

B2lt

^22t

Hor

Ap

B2lt

B22t

Hor

Ap

B2H

B22t

Depth(cm)

0-23

23-64

64-102

pH(l

H2O

5.3

4.7

4.7

Na

0.07

0.08

0.05

Fine Earth (%)

Clay

45.8

34.9

66.6

:1)

KC1

4.1

3.7

3.7

K

Silt

46.2

62.1

31.4

Sand

8.00

3.00

2.00

Ext. A Exch.

meq/100

11.2

13.3

14.4

Bases

Mg

meq/100 g soil

0.08

0.08

0.06

0.69

0.23

0.15

1.44

4.72

4.88

Ca

2.56

0.87

0.60


Sand (%)

I VFS

0.61

0

0

A Al

gsoil

0.89

3.74

4.08

2 Bases

3.40

1.25

0.86

FS

0.95

0.26

0.17

Al.S

%

21

75

83

B.S

%

25

8

6

MS CS

1.28 2.56

0.52 1.24

0.29 0.68

Fe2O3 O,C

% %

0.07 1.49

0.07 0.42

0.07 0.34

CEC

NH4OAC

meq/100 g

13.8

15.4

15.0

VCS

2.56

1.04

0.80

N

%

0.05

0.09

0.06

NH4CI

soil

8.60

15.4

14.6

VFS%

Sand

7.62

0

0

C/N

29.8

4.7

5.7

App.CECmeq/

100 g

30.1

44.1

22.5

82


PROFILE 12: KERAYONG SERIES

Hor

Ap

B21

B22

B23

Hor

Ap

B2 l

B22

B 2 3

Hor

Ap

B21

B22

B23

Depth(cm)

0-20

20-59

59-102

102-150

PH(1

H2O

4.3

4.8

4.6

4.9

Na

0.07

0.07

0.07

0.07

Fine Earth (%)

Clay

20.6

28.6

39.9

49.9

:1)

KC1

3.6

3.8

3.7

3.8

K

meq/100

0.22

0.02

tr

tr

Silt

36.4

34.6

33.6

28.8

Sand

43.0

36.8

26.5

21.3

Ext. A Exch. A

meq/100 g soil

15.2

8.82

13.4

15.1

Bases

Mg

gsoil

0.21

0.05

0,05

0.06

3.12

3.60

4.08

4.32

Ca

0.43

0.20

0.19

0.23


Sand ('

VFS

26.2

20.7

15.4

10.1

Al

2.35

2.79

3.38

3.44

Bases

0.93

0,34

0,31

0.36

FS

14.7

14.4

9.76

9.30

A1.S

%

72

89

92

91

B.S

%

12

4

5

4

MS

1.20

1.05

0.67

1.35

Fe 2 O 3

%

0.57

0.86

1.36

2.47

cs

0.63

0.50

0.41

0.25

, O.C

%

2.45

0.94

0.33

0.25

CEC

NH4OAC

meq/100

7.60

7.80

6.00

10.0

vcs

0.10

0.22

0.20

0.10

N

%

0.20

0.11

0.11

0.07

NH4CI

g soil

2.20

4.40

4.60

7.10

V F S %

Sand

60.9

56.3

58.1

47.4

C/N

12.3

8.5

3.0

3.6

App.CECmeq/

100 g

36.9

27.3

15.0

20.0

83



Hor

Ap

AC2

AC2

AC3

Hor

Ap

AC2

AC2

AC3

Hor

Ap

AC!

AC2

AC3

Depth(cm)

0-24

24-75

75-123

123-133

pH(l

H2O

4.8

5.0

4.9

4.7

Na

0.07

0.07

0.07

0.07

Fine Earth (%)

Clay

7.46

11.1

11.9

9.19

:1)

KC1

4.1

4.3

4.3

4.2

K

Silt

4.97

2.54

2.92

2.11

Sand

87.6

86.4

85.2

88.7

Ext. A Exch. A

meq/lOOg

6.30

5.54

4.60

4,96

Bases

Mg

meq/lOOg soil

tr

tr

tr

tr

0.04

0.01

0.01

0.02

1.68

1.52

1.20

1.36

Ca

0.41

0.20

0.15

0.17


Sand (%)

VFS

2.95

2.75

3.65

1.76

Al

soil

1.40

L12

0.84

0.89

£ Bases

0.52

0.28

0.23

0.26

FS

21.2

16.5

17.9

10.5

Al.S

%

73

80

79

77

B.S

%

9

7

8

13

MS CS

31.1 27.5

26.7 29.6

27.3 26.5

20.6 32.5

Fe2O3 O.C

% %

0.36 1.47

0.29 0.73

0.29 0.27

0.36 0.13

CEC

NH4OAC

meq/100

6.00

3.80

2.80

2.00

vcs

4.64

10.7

9.65

24.0

N

%

0.14

0.04

0.06

0.04

NH4CI

gsoil

2.80

2.20

2.00

1.60

VFS%

Sand

3.37

3.18

4.28

1.98

C/N

10.5

18.3

4.5

3.3

App.CECmeq/

100 g

84.4

34.2

23.5

21.8

84


PROFILE 14: RASAU SERIES

Hor

Ai

B21

B22

B23

B24

Hor

Ai

B21

B22

B23

B24

Hor

Ai

B21

Bn

B23

B24

Depth(cm)

0-10

10-33

33-85

85-118

118-128

pH(l

H2O

4.2

4.4

4.6

4.7

4.8

Na

0.12

0.07

0.10

0.10

0.10

Fine Earth (3

Clay

16.7

19.1

17.1

21.9

21.8

:1)

KC1

3.5

3.9

4.0

4.0

3.9

K

Silt

28.7

29.7

34.1

30.9

28.6

t)Sand

54.6

51.2

48.8

47.2

49.6

Ext. A Exch. A

meq/100 g soil

16.6

5.50

4.24

3.98

4.18

Bases

Mg

meq/lOOgsoil

0.18

0.04

0.02

tr

tr

0.04 0.04

0.04

0.04

0.03

0.03

4.16

2.88

2.64

2.72

2.32

Ca

0.17

0.25

0.23

0.23

0.34

Particle Size

VFS

15.5

16.9

16.2

16.0

16.4

AI

3.13

2.51

1.98

2.21

1.73

Bases

0.51

0.40

0.39

0.36

0.47

FS

26.7

25.1

23.5

21.3

24.4

Al.S

%

86

86

84

86

79

B.S

%

4

7

8

9

12

Analysis

SandC

MS

9.44

7.15

6.58

6.62

6.52

Fe2O3

%

tr

tr

tr

tr

tr

Wcs

2.75

2.00

1.99

2.42

2.10

O.C

%

3.95

1.33

0.54

0.23

0.14

CEC

NH4OAC

VCS

0.27

0.60

0.52

0.89

0.67

N

%

0.22

0.10

0.07

0.06

0.06

NH4CI

meq/100 g soil

11.6

5.80

4.60

4.20

4.00

6.00

5.00

3.80

4.00

3.60

VFS%

Sand

28.4

33.0

33.2

33.9

33.1

C/N

18.0

13.3

7.7

3.8

2.3

App.CECmeq/

100 g

69.5

30.4

26.9

19.2

18.3

85


PROFILE 15: NAPAI SERIES

Hor

An

Ai.cn

B22tcn

B23tcn

Hor

An

Ai2cn

B21tcn

B22tcn

B23tcn

Hor

An

Ai2cn

B21 ten

B22tcn

B23tcn

Depth(cm)

0-13

13-30

30-55

55-90

90-100

pH(l

H2O

4.4

4.6

4.7

4.7

4.9

Na

tr

tr

tr

tr

0.02

Fine Earth fl

Clay

12.2

16.5

39.6

40.9

53.1

KC1

3.7

3.8

3.8

3.9

3.9

K

Silt

19.6

17.8

10.8

8.91

14.6

t)Sand

68.2

65.7

49.6

50.2

32.3


Sand(

VFS

23.8

17.3

9.37

7.48

12.4

Ext. A Exch. A Al

meq/100 g soil

5.02

5.00

7,24

7.34

6.96

Bases

Mg

meq/100 g soil

0.10

0.09

0.08

0.09

0.09

0.38

0.11

0.09

0.08

0.11

1.92

2.24

4,00

3.60

4.24

Ca

0.54

0.07

0.21

0.20

0.33

1.17

1.56

3.34

3.05

3.36

2 Bases

1.02

0.27

0.38

0.37

0.55

FS

35.1

26.4

11.9

9.37

9.29

Al.S

53

85

90

89

86

B.S

20

6

8

7

11

MS

5.39

4.76

2.42

2.58

1.60

F«2O:

1.25

2.28

3.96

6.10

4.89

%)

cs

0.98

1.18

1.84

3.58

1.24

3 O.C

1.68

0.50

0.46

0.31

0.32

CEC

NH4OAC

ves

2.93

16.1

24.0

27.1

7.84

N

0.11

0.07

0.07

0.07

0.06

NH4CI

meq/100 g soil

5.20

4.88

4.80

5.44

4.94

2.80

3.36

3.52

5.20

4.80

VFS%

Sand

34.9

26.3

18.9

14.9

38.4

C/N

15.3

7.1

6.6

4.4

5.3

App.CECmeq/

100 g

42.6

29.6

12.1

13.3

9.30

86

SOME T 2 TERRACE SOILS OF PENINSULAR MALAYSIA - I

PROFILE 16: CHUPING SERIES

Hor

Ai

Bait

B22tcn

HB3

c

Depth(cm)

0-14

14-35

35-63

63-73

73+

Clay

8.36

10.7

26.5

58.5

Fine Earth (%)

Silt

38.9

32.5

24.8

23.8

Sand

52.7

56.8

48.7

17.7

Particle

VFS

27.8

23.4

13.5

8.57

Size Analysis

Sand (%)

FS

19.0

22.1

13.3

4.50

MS

4.13

6.28

5.09

1.63

CS

1.46

3.12

3.93

1.79

vcs

0.67

1.74

12.8

1.36

VFS%

Sand

52.8

41.2

27.7

48.5

Hor

A,

B2it

B22tcn

11B3

pH (1 : 1)

H2O KC1

5.3

5.3

5.6

7.4

4.1

3.9

3.8

5.8

Ext. A Exch. A AI

meq/100 g soil

8.22 1.20 0.42

9.22 2.00 1.06

11.2 3.28 2.61

0.86 0.24 0

A1.S Fe2O3 O.C

20

52

51

0

0.88

1.72

4.05

5.26

0.60

0.52

0.26

tr

N

0.07

0.06

0.06

0.06

C/N

8.6

8.7

4.3

0

Hor

Ai

B 2 1 t

B 2 1 t

B22tcn

HB3

Na

tr

tr

tr

0.04

0.54

Bases

K Mg

meq/100 g soil

0.08

0.08

0.05

0.09

0.10

0.55

0.55

0.47

1.39

11.8

Ca

1.01

1.01

0.45

0.95

8.73

2 Bases

1.64

1.64

0.97

2.47

21.2

B.S

34

34

25

18

100

CEC

NH4OAC

meq/100 g

4.80

4.80

3.84

13.4

25.2

NH4CI

soil

2.88

2.88

3.68

12.0

21.2

App.CECmeq/

100 g

57.4

57.4

35.9

50.6

43.1

87


PROFILE 17: AWANG SERIES

Hor

Ap

A3

B2

B3/BC

Hor

Ap

A3

B2

B3/BC

Hor

Ap

A3

B2

B3/BC

Depth(cm)

9-18

18-52

52-83

83-93

pH(l

H2O

5.2

5.1

4.9

4.9

Na

tr

tr

tr

tr

Fine Earth (%)

Clay

4.22

9.48

23.5

25.2

:D

KC1

4.1

4.0

3.8

3.8

K

Silt

8.03

10.4

9.95

7.79

Sand

87.7

80.1

66.5

77.0

Ext. A Exch. A

meq/100 g soil

1.84

1.42

2.30

3.32

Bases

Mg

meq/100 gsoil

0.04

0.05

0.07

0.05

0.10

0.10

0.10

0.11

0.80

1.04

2.40

2.16

Ca

0.39

0.40

0.38

0.47


Sand(

VFS

3.46

4.76

3.67

1.97

Al

0.11

0.33

1.50

1.17

Bases

0.53

0.55

0.55

0.63

FS

12.3

14.0

9.31

6.06

A1.S

17

38

73

65

B.S

76

37

23

18

MS

20.8

17.0

11.9

8.80

Fe 2 O :

%'

0.13

0.13

0.13

0.50

%)

cs

29.6

22.7

18.7

18.3

j O.C

0.42

0.26

0.10

0.03

CEC

NH4OAC

meq/100 g

2.02

1.50

2.40

3.50

vcs21.4

21.3

22.9

31.7

N

0.06

0.03

0.04

0.04

NH4CI

soil

2.00

1.40

2.35

3.40

VFS%

Sand

3.95

5.94

5.53

2.56

C/N

7.0

8.7

2.5

0.8

App.CECmeq/

100 g

47.9

15.8

10.2

13.9

88


PROFILE 18: HOLYROOD SERIES

Hor

Ap

B21t

B22t

B23t

Hor

Ap

Bat

B 2 2 t

B23t

Hor

Ap

B»«

B22t

B23t

Depth(cm)

0-18

18-35

35-70

70-90

pH(l

H2O

4.4

4.8

4.7 .

4.5

Na

tr

tr

tr

tr

Fine Earth (%)

Clay

21.2

28.6

31.7

34.6

KCl

3.7

3.9

3.8

3.8

K

Silt

10.9

8.92

8.45

8.62

Sand

67.9

62.5

59.8

56.8

Particle Size

VFS

6.30

5.00

3.90

4.04

Ext. A Exch. A Al

meq/100 g soil

6.32

5.08

5.14

4.78

Bases

Mg

meq/100 g soil

0.10

0.04

0.03

0.12

0.03

0.06

0.06

0.34

1.92

2.32

2.48

2.56

Ca

0.72

0.22

0.20

0.41

0.94

1.39

1.45

1.50

2 Bases

0.85

0.32

0.29

0.87

FS

18.7

13.4

10.3

10.7

Al.S

53

81

83

63

B.S

12

6

6

21

Analysis

Sand(%)

MS CS

20.4 17.1

14.7 14.0

12.7 18.3

11.6 15.7

Fe2O3 U.C

0.88 1.92

1.25 0.54

1.53 0.28

1.44 0,15

CEC

NH4OAC

vcs

5.25

11.2

14.3

14.7

N

0.14

0.07

0.04

0.04

NH4CI

meq/100 g soil

7.04

5.40

4.96

4.08

3.92

4.00

4.24

3.76

VFS%

Sand

9.28

8.00

6.52

7.11

C/N

13.7

7.7

7.0

3.8

App.CECmeq/

100 g

33.2

18.9

1 5 . 6

<• • 1 1 . 8

89

some t2 terrace soils of peninsular malaysia: i ... papers/pert vol. 6 (3) dec... · some t2...

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