Soil Composition Volcano Indonesia

7/28/2019 Soil Composition Volcano Indonesia

1/14

This article was downloaded by: [125.160.241.226]On: 22 April 2013, At: 02:09Publisher: Taylor & FrancisInforma Ltd Registered in England and Wales Registered Number: 1072954 Registeredoffice: Mortimer House, 37-41 Mortimer Street, London W1T 3JH, UK

Soil Science and Plant NutritionPublication details, including instructions for authors andsubscription information:

http://www.tandfonline.com/loi/tssp20

Clay mineral composition of some

volcanogenous soils in Indonesia and

the PhilippinesYasuo Kitagawa

a, Kazutake Kyuma

b& Keizaburo Kawaguchi

c

aNational Institute of Agricultural Sciences, Tokyo, Japan

bCenter for Southeast Asian Studies, Kyoto, Japan

cFaculty of Agriculture, Kyoto University, Kyoto, Japan

Version of record first published: 29 Mar 2012.

To cite this article: Yasuo Kitagawa , Kazutake Kyuma & Keizaburo Kawaguchi (1973): Claymineral composition of some volcanogenous soils in Indonesia and the Philippines, Soil Science

and Plant Nutrition, 19:3, 147-159

To link to this article: http://dx.doi.org/10.1080/00380768.1973.10432584

PLEASE SCROLL DOWN FOR ARTICLE

Full terms and conditions of use: http://www.tandfonline.com/page/terms-and-conditions

This article may be used for research, teaching, and private study purposes. Any

substantial or systematic reproduction, redistribution, reselling, loan, sub-licensing,systematic supply, or distribution in any form to anyone is expressly forbidden.

The publisher does not give any warranty express or implied or make anyrepresentation that the contents will be complete or accurate or up to date. Theaccuracy of any instructions, formulae, and drug doses should be independentlyverified with primary sources. The publisher shall not be liable for any loss, actions,claims, proceedings, demand, or costs or damages whatsoever or howsoever causedarising directly or indirectly in connection with or arising out of the use of thismaterial.
http://dx.doi.org/10.1080/00380768.1973.10432584http://www.tandfonline.com/loi/tssp20http://www.tandfonline.com/page/terms-and-conditionshttp://www.tandfonline.com/page/terms-and-conditionshttp://dx.doi.org/10.1080/00380768.1973.10432584http://www.tandfonline.com/loi/tssp20


2/14

Soil Sci. Plant Nutr., 19 (3), 147-159, 1973

CLAY MINERAL COMPOSITION OF SOME VOLCANOGENOUSSOILS IN INDONESIA AND THE PHILIPPINESYasuo KITAGAWA,* Kazutake KYUMA,** andKeizaburo KAWAGUCHI***

*National Institute of Agricultural Sciences, Tokyo, Japan,**Center for Southeast Asian Studies, andFaculty of Agriculture, Kyoto University, Kyoto, JapanReceived April 2, 1973

Clay fractions of three Andosols and a Latosol occurring in Indonesia, and twoAlluvial Soils derived from pyroclastic sediments in the Philippines were examinedby means of chemical analyses, X-ray diffraction, differential thermal analysis,thermogravimetry, infrared absorption spectroscopy, and electron microscopy. Theresults are summarized as follows .Allophane is a dominant clay mineral of young volcanogenous soils occurringin the tropics. Small amounts of halloysite, gibbsite, and imogolite are also foundin some of the young volcanogenous soils. Halloysite and imogolite are relativelyabundant in the surface soil, while gibbsite is more abundant in the subsoil. Inthe clay fraction of the young volcanogenous soils in the tropics, a-cristobalite isoften present, but quartz occurs rarely, Small amounts of feldspars are also presentin the Philippine soils. 2 : 1-type minerals are found to a small extent in some ofthe sample soils. The above results agree well with the results for JapaneseAndosols, except for a difference in the primary mineral composition.

In this paper, we term soils derived mainly from pyroclastic materials, volcano:genous soils. Andosol in FAO/UNESCO nomenclature is a well-known representativeof the volcanogenous soils.Today, Andosols are known to occur in active volcanic regions all over the world,.regardless of the climate. The most intensively studied of all, however, are thoseoccurring in the temperate zone of the Circum-Pacific volcanic region, especially injapan and New Zealand ( 1-11 ). A specific clay mineralogy of the temperate zoneAndosols has been clarified in recent years, as follows: 1) allophane. is a dominant


3/14

148 Y. KITAGAWA, K. KY UMA, and K. KAWAGUCHIsomething todo with this fact. However, very little is known about the cla y mineralogyof the tropical volcanogenous soils. RUTHERFORD and W A T A N AB E ( 12) studied th emineralogical composition of Andosols from Eastern New Guinea and found that alia-:phane was a domin ant clay mineral species, accompan ying a considerable am ount ofgibbsite in th e subsoil.In the present paper, we have attempted to clarify specificity in the clay mineralogyof the tropical volcanogenous soils, taking several profiles from Indonesia Uava) andthe Philippines, which represent the active volcanic region of tropical Asia.

SAMPLES AND EXPERIMENTAL METHODSThree profiles from Indonesia (Java) and two profiles from the Philippines wereused as the sample of young volcanogenous soils, which are supposed to have developed on Holocene pyroclastic sediments. T he three Indonesian soils are classified as Andosols

in Indonesia: IN-4 is a paddy field on a colluvium in the mid-slope of M t. Salak, avolcano having been active until recent times, whereas IN-15 and IN-30 are uplandso ils, having a humus-rich A horizon developed from recent aeolian sediments from thenear-by volcanos. All of these Andosols are loca ted on elevat ions above 600 m . Thetwo Philippine soils a re derived from sandy alluvial sedim ents consisting almost ex-clusively of pyroclastic materials.

Soil Horizon(em)

IN-1 (1) Apg 0-15(3) Blg 27-46{5) BCg 75-100+

IN -4 {1) Apg 0-16(2) Bg 16-27

IN-15 (1) AI 0-20(2) AB 20-55(4) IIIAb 85 -15 5(6) lV Ab 190-245

IN-30 (1) All 0-50{3)C l 62-83

{5-7) C3-5 105-140(10) cs 180-230+

Ph-42 (1) Apg 0-19(3) Bg 24-45

Ph54 {1) Ap 0-12(4) Bg 24-52

Color

10YR 4/46.25YR 4/67.5YR 3.5/4lOYR 2/210YR 3/17.5YR 2/1/57.5YR 3/47.5YR 1.7/17.5YR 2/1lOYR 2.5/210YR 3/27.5-10YR 2-3/2-37.5YR 3/410YR 3/12.5YR 6/3lOYR 5/25YR 5/2

Texture

HCHCHCCLCLLiCSCLLiCSLCLSCLSLSCLSLsSCLSL

Table 1 ..Organic carbon

(%)1 .65

5.605 .4 96 .596 .007.587 .405.51

3 .35

2 .56

2.7 2

Downloadedby[125.160.241.226]at02:0922April201

3


4/14

Clay Minerals of Tropical Volcanogenous Soils 1491A "reddish-brown Latosol" in Indonesian Classification, IN-1, was also taken as asample for the purpose of comparison. This soil developed on an old pyroclastic flowor an old alluvial fan deposit from Mt. Salak and Mt. Pangrango, another active volcano.Thus IN-1 may be regarded as an old volcanogenous soil from the viewpoint of parent

materials. Although this soil bears the name of Latosol and shows a reddish coloration,it still contains some unweathered colored minerals throughout the profile. The difference in the morphology, as compared with the Indonesian Andosols, is due, of course,to the time factor over which the soil has been developed and also to the intensity ofweathering which is a function of elevation, ca. 200m above M.S.L. for the reddish.brown Latosol versus >600 m for the Andosols. The location and a brief descriptionof the sample soils are given in Table 1.The fractions of clay (below 2 p) and silt (2-20 p) were separated from the soilsamples by the sedimentation method, after a hydrogen peroxide treatment. Theprepared clay and silt separates were examined by the following methods.Silicon in the sample was determined by colorimetry (molybdenum blue method)after fusion with alkali. The other elements were determined after the dissolution ofthe sample by HF HzSO, treatment. Aluminon and o-phenanthroline methods wereused for colorimetric determination of aluminum and iron, respectively. Magnesiumand potassium were determined by atomic absorption photometry and flamephotometry,respectively. Free iron oxide and free alumina in the clay fraction were determined

Samples.Materials and classification

Old alluvial fan deposits.Reddish-brown LatosolColluvium on mid-slope of Mt. Salak.AndosolRecent pyroclastic aeolian deposits.Andosol

Recent pyroclastic aeolian deposits.Andosol

Recent alluvium. Alluvial soil(Banga series)Recent alluvium. Alluvial soil(Legaspi series)

Location

Kedung Halang, Bogor, West Java,IndonesiaBlock Kramat, Afd, Sukamantri, Kotabatu, Bogor, West Java, IndonesiaBatureok, Tjikahuripan, Lembang,Bandung, West Java, Indonesia

Karangduren, Salatiga, Semarang,Central Java, Indonesia

Liwanay, Banga, Cotabato Sur,The Philippines

Land utilization

Paddy field(Double cropping}Paddy field(Double cropping}Upland field (for Vegetables)

Upland field(for Cassava)

Paddy fieldTagas, Daraga, Albay, The Philippines Paddy field


3


5/14

150 Y. KITAGAWA, K. KYUMA, and K. KAWAGUCHIby the MEHRA and JACKSON ( 13) method.X-ray diffraction patterns were obtained with Cu-Ka radiation (40 kV, 10 m A )using a Rigaku Denki, Geigerfiex Model D-6C. A specimen oriented on a glass slidewas used to emphasize 001-reflection of crystalline clay minerals, in addition' to arandom powder specimen. Differential thermal curves and weight-loss curves wereobtained by using a Shimadzu, Model TG-2B thermal analyzer, at a heating rate o fl0C/min from room temperature to 1,000C in an ordinary atmosphere. Infrared ab -sorption spectra were obtained by using a Hitachi, Model EPI-G2 infrared spectrometer.A KBr tablet was prepared by mixing 1 mg of a sample with 200mg of KBr. Electronmicrographs were taken in a Hitachi, Model HU-12 electron microscope at an accelerating voltage of 75 kV with a direct magnification of 10,000x.

RESULTS AND DISCUSSIONChemical compositions of the clay and silt fractions in Indonesian and Philippine'soils are shown in Table 2. Molecular ratios between silica and sesquioxide calculatedirom the results in Table 2 are shown in Table 3. In Indonesian Andosols, the silica:alumina molecular ratio of the clay fraction varies from 1.03 to 1.97, and the valuefor IN-4 was a little higher. In the subsoils of the two Philippine soils, silica-alumina.ratios of the clay fraction were 1.65 and 1.89, and the values for surface soils 'were

Table 2. Chemical composition of clay and silt fraction (%, air-dried basis).Soil

(horizon)Clay fraction

1N1 (1) 35.1 31. 8 11. 7(3) 32.9 30.9 11.5(5) 33. 9 30. 1 11. 2

lN-4 (1) 33.2 29.4 5. 5(2) 29.7 25.6 8.8

JN-15 (1) 23. 5 28. 5 11. 3(2) 22.5 27.9 12.2(4) 21.4 27.8 11.0(6) 19.4 30.1 12.7

JN-30 (1) 24.2 30.3 8. 4(3) 22. 8 30. 2 8. 1(5) 21. 6 31. 9 8. 4

(10) 20.0 33.0 10.3Ph-42 (1) 40. 6 23. 6 6. 0

(3) 28. 4 29. 3 5. 6Ph-54 (1) 48.6 21.0 4. 7

(4) 28.2 25.3 12.2

0.10.10.10.30.20.20.20.20.10.10.10.10.20.40.30.20.3

0.1 20. 8 99. 60.1 23.7 99.20. 1 23. 7 99.10.1 30.8 99.30.1 34.8 99.20.1 35.4 99.00.'1 36.8 99.7o. 1 39. 1 99. 60.1 37.2 99.60.2 36.4 99.60.1 38.1 99.40.1 37.4 99.50. 1 35. 5 99. 10.1 28.6 99.30.1 36.0 99.70.1 24.7 99.30.1 33.0 99.1

Silt fraction

43.2 29.8 11.236.3 29.1 13.438.8 30.6 11.358.1 18.5 7.261.7 12.3 9.852.8 19.2 8.942.2 22.6 10.741.0 21.8 11.034.1 23.3 13.645.6 24.2 7.233.4 25.2 8.528.6 31.3 8.525.0 30.0 11.073.5 10.2 3.548.4 24.3 5.467.9 17.3 3.545.9 23.3 8.7

0. 2 0. 2 14. 6 99. 2 .0.1 0. 2 20. 2 99. 30.1 0.1 18.5 99.41. 3 0. 4 13. 8 99. 3 '1.5 0.5 13.8 99.60.4 0.4 17.7. 99.40. 3 0. 4 23. 3 99. 50.3 0.3 25.4 99. s0.2 0.3 27.7 99 .20. 3 o. 6 21. 2 . 99. 10.2 0.5 31.4 99.2o. 2 o. 4 30. 1 99. 10. 3 0. 3 33. 0 99. 61.0 0.6 10.7 99.51. 2 0. 7 19. 3 99 . 31. 1 0.5 9.2 99.51. 2 0. 4 19. 8 99. 3


3


6/14

Clay Minerals of Tropical Volcanogenous Soils 1StTable 3. Molecular ratios of clay and silt fraction.

Soil Clay fraction Silt fraction(horizon) Si0 2/AI 203 Si0a/Ra03 Si0a/Ala03 Si02/Ra03IN-1 (1) 1.87 1.52 2.46 1.99

(3) 1.81 1.46 2.12 1. 64(5) 1.92 1.55 2.15 1. 74

IN-4 (1) 1. 92 1.72 5.34 4.28(2) 1. 97 1.61 8.56 5.66

IN-15 (1) 1. 40 1.12 4.68 3.61(2) 1. 37 1.07 3.16 2.43(4) 1.30 1.04 3.19 2.41(6) 1.10 0.86 2.48 1. 80IN-30 (1) 1. 36 1.15 3.20 2.69(3) 1.28 1.09 2.25 1. 85(5) 1.15 0.98 1.55 1. 32

(10) 1. 03 0.86 1. 41 1.15Ph-42 (1) 2.93 2.52 12.23 10.03

(3) 1.65 1.47 3.38 2.96Ph-54 (1) 3. 93 3.44 6.65 5.89

(4) 1.89 1.45 3.34 2.69

considerably higher. The silica-alumina ratio of the clay fraction was lower than thatof the silt fraction. The silica-alumina molecular ratio of subsoil seemed to be lowerthan the value for surface soil in the clay and silt fractions. The silica-alumina ratio.of tropical volcanogenous soils appeared to be in the same order as that for Japanese.Andosols ( 7 ). Iron content in the tropical soils examined was not higher than that in.Japanese Andosols ( 7 ). In the case of Indonesian Andosols, the iron content of the.silt fraction was a little higher than that of the clay fraction. The same holds for the.Latosol, IN-1. In the Philippine soils, however, the iron content of the clay fraction.was higher than that of the silt fraction. The contents of magnesium and potassium.in the clay fraction were lower than those in the silt fraction. Magnesium contents.of IN-4, Ph-42, and Ph-54 were slightly higher than those for the other soils. Magnesium and potassium contents in the clay fraction of the tropical volcanogenous soilswere generally lower than those in Japanese Andosols, which contain 0.2Q-2.28% ofmagnesium and 0.03-2.13% of potassium ( 7). The content of total water in the clayfraction was high in Indonesian Andosols but comparatively low in IN-1 and in the.surface layer of the Philippine soils. Water contents of the silt fraction in IN-15 andIN-30 were also quite high. The high content of total water in Andosols suggests an..abundant presence of allophane.X-ray diffraction patterns obtained from the powder specimens of clay and osilt.fractions are shown in Figs. 1 and 2. In all the horizons of IN-1, a reddish-brown.


3


7/14

152 Y. KITAGAWA, K. KYUMA, and K. KAWAGUCHIIN IS

INl

2 A 5 4 3 2 A 1410 7 5 4 3 2 1410 7 5 4 3 2 A:Fig. 1. X-ray diffraction patterns of clay and silt fraction in Indonesian soils (powder method).

Fig. 2. X-ray diffraction patterns of clay and silt fractionin Philippine soils (powder method).

Latosol derived from old pyroclastic materials, the reflections at 7.3 A (doo!), 4.45 A(dozo), and 3.6A (dooz), originating in kaolin minerals, were found clearly. Judging fromthe value of d o o ~ o the kaolin mineral was identified as halloysite, which was also confirmed by electron microscopy, thermal analyses, and infrared absorption spectroscopy{Figs. 4, 6). Quartz (3.35 A} and a-cristobalite (4.06 A) were detected in the silt fractionof IN-1, but not in clay fraction. Small amounts of gibbsite (4.83 A} and 2 : 1-tyPeminerals (14 A) were found in the surface soil and the subsoil of IN-1, respectively{Figs. 1, 3).The clay fraction of the young volcanogenous soils consisted mainly of allophane.-amorphous to X-ray, and the silt fraction also contained predominantly amorphousmatter. In the surface soil of IN-4, Ph-42, and Ph-54, the powder specimens of theday fraction showed a reflection at 4.45 A associated with dozo of layer silicate. .Theweak reflections at 7.3 A and 14.5 A in the oriented specimen of Ph-42 may originatein halloysite and the 2: 1-type minerals, respectively (Fig. 3}. Halloysite with a 7.3 A


3


8/14

Clay Minerals of Tropical Volcanogenous Soils 153

IN-1(1)

IN-1(5)

Ph-42(1)

Pb-541.1)

Fig. 3. X-ray diffraction patterns of oriented clay specimens.

reflection was contained in Ph-54 (Fig. 3); this was also confirmed in an electronmicrograph (Plate 4). The very weak d001 reflection in the oriented specimen of IN-4,despite the presence of do2o, may indicate that the layer silicate in IN-4 is a randomlymixed-layer mineral ( 14 ). A considerable amount of gibbsite was found in IN-30, and.it was comparatively abundant in the subsoil. This agrees well with the result obtained for Andosols in Japan and New Guinea, as mentioned above. The clay fraction.of IN-30, contained a-cristobalite in the surface soil. Feldspars were detected in the-clay fraction of the Philippine soils. Primary minerals in the clay fraction are lumpedtogether and are shown in Table 4. In the silt fraction of Andosols, reflection at 4.06A, originating in a-cristobalite, was found clearly in all samples. Feldspar (3.20 A) was.also found commonly in silt fractions, and was comparatively abundant in IN-4, Ph-42,and Ph-54. Quartz was contained relatively little in clay and silt fractions of all samplesoils. In this, the tropical volcanogenous soils examined herein are different from mostof the Japanese Andosols. Differential thermal curves, weight-loss curves, and the infrared absorption spectra-of the clay fraction are drawn in Figs. 4-7. The differential thermal peaks at 120-130, 550, and 930C in IN-1 appeared to be associated with halloysite. This was alsosuggested by the weight-loss curve. A small amount of gibbsite was detected by thedifferential thermal curve of IN-1 (Fig. 4). The differential thermal curve and weightloss curve showed an allophane type except in the case of the surface soil of Ph-54(Figs. 4, 5). The curves for the surface soil of Ph-54 had an endothermic peak andweight l o ~ s near 50


9/14

154 Y. KITAGAWA, K. KYUMA, and K. KAWAGUCHITable 4. Mineralogical composition of clay fraction (%, oven-dried basis).

Soil Clay miner. Sesquioxides Primacy miner.(horizon) Allo. Kao. Gib. free AI203 Goe. Qz. Cri. Fd.IN-1 (1) 11 72 4 2 11

(3) 12 72 4 2 10(5) 12 73 3 2 10

IN-4 (1) 88 5 4 3 + (2) 80 5 5 10IN-15 (1) 72 8 5 15

(2) 72 7 5 16 (4) 77 4 5 14 +(6) 70 7 2 5 16 +IN-30 (1) 77 4 2 6 11 + (3) 80 tr . 3 5 11 + (5) 77 tr . 5 5 12 + (10) 63 tr . 20 4 12 + +

Ph-42 (1) 90 tr . 5 4 + +(3) 90 5 5 + +Ph-54 (1) 77 20 2 tr . + +(4) 80 4 16 + +1) Allo., allophane (containing imogolite and free silica) : Kao., kaolin minerals; Gib., gibb-site: Goe., goethite; Qz., quartz; Cri., cristobalite; Fd., feldspar.

Fig. 4. Differential thermal curves and weight loss curves of clay fraction in Indonesian s o i l s ~ '


3


10/14

Clay Minerals of Tropical Volcanogenous Soils

4 6 8 10X OO'CFig. 5. Differential thermal curves and weight loss curves of clayfraction in Philippine soils.

Fig. 6. Infrared abso'rption spectra of clay fraction in Indonesian soils.

Fig. 7. Infrared absorption spectra of clay fraction in Philippine soils.

155

and weight loss near 500C. The differential thermal peak and weight loss at 300Cdue to gibbsite were conspicuous for IN-30, and they were larger for the subsoil thanfor the surface soil sample. A small amount of gibbsite was also found in the subsoilof IN-15.


3


11/14

156 Y. KITAGAWA, K. KYlJMA, and K. KAWAGCCHI

Plate 1. Electron micrograph of clay specimen in IN-4(1) (The symbol indicates a length of 1 p ) .

Plate 2. Electron micrograph of clay specimen in IN-30(1) (The symbol indicates a length of 1 p ).


3


12/14

Clay Minerals of Tropical Volcanogenous Soils 157

Plate 3. Electron micrograph of clay specimen in Ph-42(1) (The symbol indicates a length of 1 p.).

Plate 4. Electron micrograph of clay specimen in Ph-54(1) (The symbol indicates a length of 1 p) .


3


13/14

158 Y. KITAGAWA, K. KYUMA, and K. KAWAGUCHIThe broad bands of infrared absorption spectra near 3,450, 1,630, 1,000, and 55()cm-1 found in the Indonesian Andosols and the Philippine soils may originate in allophane (Figs. 6, 7). The absorption bands at 3,690 and 3,610 cm-1 found in IN-1 maybe associated with the stretching vibration of the hydroxyl group in halloysite (Fig. 6).

The absorption bands at 3,600, 3,510, 3,450, and 3,370 cm-1 found in the subsoil o fIN-30 may originate in gibbsite. The infrared absorption spectrum of Ph-54 indicates.the presence of kaolin minerals, especially in the far-infrared region.Tubular particles of halloysite were observed in the clay fraction of IN-1 by electronmicroscopy. In the electron micrograph of IN-4, sheet-like particles probably associatedwith 2 : 1-type minerals were found besides allophane particles (Plate 1); this was alsoinferred from the result of X-ray diffraction. Particles like a grape tuft associatedwith allophane were plentifully observed in electron micrographs of IN-15 and IN-30.A small amount of imogolite, which is fibrous in appearance ( 15), was observed in th esurface soil of IN-30. (Plate 2). A scanty presence of imogolite was also confirmed inthe surface soil of IN-4, IN-15, and Ph-42. A small amount of halloysite besides allophane was found in an electron micrograph of Ph-42 (Plate 3). The clay fraction inthe surface soil of Ph-54 consisted of allophane and halloysite (Plate 4), as mentionedearlier. The electron micrograph of Ph-54 showed the shape of halloysite particles aseither tubular or onion-like. The presence of halloysite and 2 : 1-type minerals in th esurface soil of IN-4, Ph-42, and Ph-54 might be caused by contamination by non-pyroclastic materials in the process of colluviation and alluviation.The mineralogical composition of each clay fraction was summarized from theabove results, as shown in Table 4. The contents of kaolin minerals and gibbsite werecalculated from weight losses in the thermogravimetry ( 16). The content of kaolinmineral is 7.16 times the weight loss at 500-600C, because the content of structuralwater released at this temperature is 13.96% based on the formula, Al2SizO$(OH),, Thecontent of gibbsite is 2.89 times the weight loss at 3000C. Water content of gibbsite(Al(OH)a) is assumed to be 34.65%. The contents of goethite and free alumina werecalculated from the amounts of iron and aluminum removed in the treatment with th eMEHRA and JACKSON method ( 13 ). Goethite (FeOOH) is 1.11 times the content o fFe20 8 The content of allophane was determined indirectly by subtracting the sum o fkaolin mineral, gibbsite, geothite, and free alumina from 100%. Imogolite and freesilica were included in allophane, because it is difficult to separate them. For IN-1.IN-4, and Ph-42, 2: 1-type minerals were too insensitive in the thermal reaction to be-determined, so that they were, if any, included in either kaolin mineral or allophane.Primary minerals may be negligible, judging from the result of X-ray diffractionanalysis.Halloysite was prevalent in the Latosol, IN-1; while allophane was dominant in th eyoung volcanogenous soils. A gibbsite content as high as 20% in the subsoil of IN-30and a halloysite content amounting to 20% in the surface soil of Ph-54 may warrant.special mention.

Acknowledgement. IW are grateful for the help extended by the Bureau of Soils, The Republic


14/14

Clay Minerals of Tropical Volcanogenous Soils 159.and Mr. Nagao Okagawa participated in the field work an d Mr. Okagawa and Mr. Prachak Charoen.carried out chemical as well as preliminary clay mineralogical analyses of the sample soils. Helpful.advice given by Dr. Yutaka Watanabe, National Institute of Agricultural Sciences, in the course.of the preparation oi the present paper is deeply appreciated.

REFERENCES1) AoMINE, S. and YosHINAGA, N., Soil Sci., 79, 349 (1955).2) AoMINE, S. , J, Sci. Soil Manure, JaPan, 28, 508 (1958)3) BIRREL, K.S. an d FIELDES, M., J, Soil Sci., 3, 155 (1952)4) EGAWA, T., WATANABE, Y., and SoTO, A., Bull. Nat. /nst. Agr. Sci., B5, 39 (1955)5) FrELDES, M., New Zealand J, Sci. Tech., Section B, 37, 336 (1955)6) KANNO, I. , Adv. Clay Sci., 1, 213 (1959)7) KANNO, I. , Bull. Kyushu Agr. E:cpt. Sta., 7, 1 (1961)8) KURABAYASHI, S. and TSUCHIYA, T., Adv. Clay Sci., 2, 178 (1950)9) KUWANO, K. and MATSUI, T., Misc. Repts. Res. Inst. Nat. Resources, 45, 33 (1957)10) MATSUI, T., Adv. Clay Sci., 2, 229 (1950)

11) Suno, T., "Mineralogical Study on Clay of Japan," Maruzen, Tokyo, pp. 328 (1959)12) RUTHERFORD, G.K. and WATANABE, Y., Proc. Intern. Clay Con/., 1956 Jerusalem, I, 203 (1955)13) MEHRA, O.P., and JACKSON, M.L., Clays Clay Miner., 7, 317 (1959)14) Suno, T., "Clay Minerals (New Ed.), Iwanami, Tokyo, pp. 300 (1966)15) YosHINAGA, N. and AOMINE, S. , Soil Sci. Plant Nutr., 8, 22 (1952)16) WATANABE, Y. and SUGO, S. , Abs. Ann. Meet. Soc. Sci. Soil Manure, Japan, 18, 41 (1971)


3

Documents

Soil Composition Volcano Indonesia