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¬­ *ῌT ®¯*ῌ°±¨²*ῌ³´*ῌTµ¬**Soil Environment Monitoring by Multi-frequency Electromagnetic Sounding
Yuuya HIRAI*, Yasushi MORI*, Hiroaki SOMURA*, Naokazu EGUSA* and Taihei MORISAWA*** Faculty of Life and Environmental Science, Shimane University,+*0* Nishikawatsu, Matsue 03*ῌ2/*., Japan** The United Graduate School of Agricultural Sciences, Tottori University,.ῌ+*+ koyama-minami, Tottori 02*ῌ2//-, Japan
Abstract
Surface soil environment was surveyed and characterized using a multi-frequency electromagnetic wave (EM) sensor.

Traditional resistivity method needs multiple point electrodes in theﬁeld to investigate the deeper points, however, this method uses broadband electromagnetic data
to obtain the apparent conductivity from di#erent depth, i.e., the higher the frequency, theshallower data we can obtain. It is non-invasive and rapid, therefore, appropriate for wide area
environmental survey.

Five frequencies of ,-+*, -21*, 13/*, ,./+* and .131* Hz were applied sothat we obtained vertical proﬁle of the domain. Forest under di#erent management, winterponded paddy ﬁeld, orchard and tea farm in hilly mountainside and orchard in plain ﬁeld were
investigated using a broadband electromagnetic wave sensor sounding.

Surface electrical con-ductivity (EC) obtained by Wenner array has the highest correlation with .131*Hz data, showing
it is the appropriate frequency for surface soil investigation. Moreover, EC in the order of several
tens milli-Siemens obtained by EM sounding corresponded very well with the EC obtained bytraditional method. Conductivity data successfully showed management induced changes insoil environment by conductivity map along with vertical conductivity proﬁle, which is advantage of broadband EM survey.

Water content changes in forest after rainfall, e#ect of ponding

management in paddy ﬁeld, and the di#erences in fertilizer application practice in hilly farm,
were clearly demonstrated by the broadband EM sensor.
Key words : Electromagnetic wave sounding, nondestructive investigation, Electrical conductivity.

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

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Soil physical properties of examined ﬁeld4

Forest West

Forest South

Paddy ﬁeld

Tea farm

Brown forest
soils

Brown forest
soils

Gley paddy
soils

Red-Yellow
soils

Red-Yellow
soils

Red-Yellow
soils

Sampling point

,*

,+

,+

,/

,+

+,

Sampling Depth (cm)

+*

+*

+*

+*

+*

+*

EC+ : / (mS m+)+.41- .400

+142, +41-

+/4*1 -4,3

.+4/- .430

++42. *4-1

-4*/ *4*3

Moisture ratio (g g+)

*4-2 *4+2

*4.0 *4+*

*4.+ *4*/

*4/- *4+0

*4-+ *4*+

*4-- *4*.

VWC (m- m-)

*4-3 *4+.

*4.- *4++

*4., *4++

*4/2 *4+/

*4,3 *4*/

*4-, *4*.

Bulk density (Mg m-)

+4*1

*43/

+4.,

*43/

*43/

+4*2

Soil Hardness (kg cm,)+4*3 *40/

+431 *43,+400 *4.0

-40, +4..

/4-0 +4.,

Soil

Orchard (hilly) Orchard (plain)

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Forest South,4-0

Paddy ﬁeld Tea farm Orchard (hilly) Orchard (plain)
+-4+2
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143*
.042,
Unit : m
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24.2
14.+
+*4,0
2430
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14,0
2401
++402
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Depth of investigation estimated from soil conductivity4

Land Management Forest WestElectrical*4,+
conductivity (mS m+)Frequancy (Hz)
.131*
,./+*
13/*
-21*
,-+*

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241,
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Comparison of EC between traditional Wenner array measurement and multi-frequency EM survey

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(a) Forest West, (b) Forest South, (c) Tea farm, (d) orchard (plain), (e) orchard (hilly), (f)Paddy ﬁeld! " f #$-.8'()9: ; <=0 c d =>?)*'# @A*BC)DE

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10

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Vertical EC map obtained by multi-frequency EM survey.
(a) Forest West, (b) Forest South, (c) Tea farm, (d) orchard (plain), (e) orchard (hilly), (f) Paddy
ﬁeld (Before Inundation), (g) Paddy ﬁeld (After Inundation)

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11

!

Vertical EC map of before and after rain in the forest obtained by multi-frequency EM survey.
(a) Forest West (Before rain), (b) Forest West (After rain), (c) Forest South (Before rain), (d)Forest South (After rain)

῍ῌTable -&'()*+,-

Volumetric water content changes before and after rainfall4
GEM-,.EC data at.131* Hz [mS m+]Site

Rainfall

Sampling
Depth (cm)West

before
after

+*
+*

*4+20
*4,,3

*4+10!
*4+-*!

*4,*1
*4.1*

*4,2-!
*4/23!

South

before
after

+*
+*

*4,*1
*4,/-

*4*/+!
*4*03!

,4-0,
,40,0

,4*0.!
,4*-+!

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a$ bQcd5efg

W2/ h*ijkl

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45Ox/

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9pqrs&9t

u&vw

u /
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12

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Table .



Ion chromatography of + : / soil extracted water4

Sampling Depth (cm)Forest West+*

Forest South+*PO. -
F
Cl
NO, Unit : mg L+
Br
NO-
SO.,

+243,
N4D4
04.,
+41*
*4.2
/410
+*421

+343+
N4D4
/4+,
N4D4
*4/2
*4.,
,*4/-

Paddy ﬁeld Tea farm Orchard (hilly) Orchard (plain)
+*
+*
+*
+*
,-4*/
N4D4
+4.
*4,
N4D4
+/41
,.4,

2-4/
N4D4
,42
N4D4
*4,/4.
./43@A"B$CD!"#$ "  ,-

@A" E @) 6%6 F*-1 

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

+340
*4*4/
N4D4
N4D4
,4/
,41

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N4D4
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J. Jpn. Soc. Soil Phys.
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Calibration of Temperature Dependence of a Dielectric Probe
Tadaomi SAITO*, Haruyuki FUJIMAKI** and Hiroshi YASUDA**** Arid Land Research Center, Tottori University & Research Fellow of JSPS (PD),+-3* Hamasaka, Tottori, Tottori, 02*ῌ***+, Japan** Graduate School of Life and Environmental Sciences, University of Tsukuba,+ῌ+ῌ+ Tennodai, Tsukuba, Ibaraki -*/ῌ2/1,, Japan*** Arid Land Research Center, Tottori University,+-3* Hamasaka, Tottori, Tottori, 02*ῌ***+, Japan
Abstract
An empirical calibration method for temperature dependence of a commercially available
capacitance probe (ECH,O probe : Decagon Devices) was presented in this paper.

A laboratory

experiment was conducted to obtain probe outputs at di#erent water contents (q) and temperatures (T) using soil from Shaanxi Province, located in the Loess Plateau, China.

The probe output

showed strong positive response to T. A calibration equation describing the probe output as afunction of q and T was developed through an empirical curve ﬁtting approach. The q values
were estimated by solving the calibration equation numerically. The root mean square errors
between actual and estimated q were *.*+0 m- m-.

We also discussed the theoretical backgroundof the temperature dependence of the probe using the results from the experiment.
The calibration equation was applied to ﬁeld observation data in the Loess plateau. The
equation signiﬁcantly reduced the daily and seasonal ﬂuctuations of the probe outputs to T. A
linear calibration equation provided by the manufacturer, which neglects temperature dependence, caused incorrect interpretation of water movements, suggesting the importance for temperature calibration in arid environments.
Key words : dielectric probe, temperature dependence, calibration, water content, Loess plateau

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18

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19

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20

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22

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Inc. Application Note. AN1*TP-+*. Decagon Devices

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Inc., Pullman, Wash.

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Campbell, C.S. (,**,) : ECH,O Dielectric Probes vs Time

Christensen,

N.B.

(,**/) : Irrigation

management

using soil moisture monitors. Western Nutrient

21 8cv9T;

Management Conf. 0 : .0῎/-. Salt Lake City, UT.

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Czarnomski, M.N., G.W. Moore, T.G. Pypker, J. Licata  _Qa

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water content in two forest soils of the Paciﬁc
Northwest. Can. J. For. Res., -/ : +201῎+210.
Decagon Devices, Inc. (,**0) : ECH,O Soil Moisture
Sensor Operator’s Manual For Models EC-,*, EC+*, and EC-/ Version ,.,, Decagon Devices Inc.,
Pullman, WA.
Fares, A. and V. Polyakov (,**0) : Advances in cropwater management using capacitive water sensors.
Adv. Agron., 3* : .-῎11.

¨'ῌ©FªῌHiE ῌ«¬ῌ­® ¯
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tric and electrical conductivity measurement

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Jones, S.B. and D. Or (,**,) : Surface area, geometr-

using time domain reﬂectometry. Vadose Zone J.
, : ...ῌ.1/.

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].^._`ab1cCdeEfg h ./ iJK

ical and conﬁgurational e#ects on permittivity#LMN#$5fgjNfgON ,-ῌ,2.

of porous media. Journal of Non-Crystalline Solids,

PQRῌPklmῌnop ,**/ : ECH,O q-*/ : ,.1ῌ,/..
Jones, S.B. and D. Or (,**-) : Modeled e#ects on permittivity measurements of water content in highsurface area porous media. Physica B, --2 : ,2.ῌ,3*.
Luedeling, E., M. Nagieb, F. Wichern, M. Brandt, M.

.,2 . rs1t.uvwx#$ῌyz{%&  7| +1 }JK#LMN~O2*2ῌ2*3.
Schwank, M. and T.R. Green (,**1) : Simulated e#ects
of soil temperature and salinity on capacitance

Deurer and A. Buerkert (,**/) Drainage, salt

sensor measurements. Sensors, 1 : /.2ῌ/11.

leaching and physico-chemical properties of ir-

Seyfried, M.S. and L.E. Grant (,**1) : Temperaturerigated man-made terrace soils in a mountaine#ects on soil dielectric properties measured at

oasis of northern Oman. Geoderma, +,/ : ,1-ῌ,2/.

/* MHz. Vadose Zone J. 0 : 1/3ῌ10/.

McMichael, B. and R. J. Lascano (,**-) : Laboratory
evaluation of a commercial dielectric soil water
sensor. Vadose Zone J., , : 0/*ῌ0/..

>ῌL ῌ +310 : Mxv

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ADR/01 U MN£ .* : /*3ῌ/+3.
Or, D. and J.M. Wraith (+333) Temperature e#ects on-,ῌ--.
Topp, G.C., J.L. Davis and A.P. Annan (+32*) : Electro-

soil bulk dielectric permittivity measured bymagnetic determination of soil water content :time domain reﬂectometry : a physical model.

measurements in coaxial transmission lines. Water

Water Resour. Res., -/ : -1+ῌ-2-.
Pepin, S., N. J. Livingston and W.R. Hook (+33/) :Resour. Res., +0 : /1.ῌ/2,.
Verstricht, J., B. Neerdael, P. Meynendonckx and G.

Temperature dependent measurement errors in

Volckaert (+33.) : Clay moisture measurements

time domain reﬂectometry determinations ofin radioactive waste disposal research. Proceed-

soil water. Soil Sci. Soc. Am. J., /3 : -2ῌ.-.

ings of the symposium on time domain reﬂecto-

Petersen, L.W., O.H. Jacobsen., F., Plauborg., M. An-

metry in environmental, infrastructure, anddersen and D.E. Rolston (+33/) : The e#ects ofmining applications, Evanston, Illinois, Sept 1ῌ3,

temperature on the determination of soil water

U.S. Bureau of Mines, special publication SP +3ῌ

content by time-domain reﬂectometry, paper
presented at Soil Sci. Soc. Am. Annual Meeting,
St. Louis, Mo., Oct.,3 to Nov. -.

3., NTIS PB3/ῌ+*/123, --1ῌ-.2.
Weast, R.C. (Ed.) (+320) : Handbook of Chemistry andPhysics. CRC Press,Boca Raton, FL.

Regalado, C.M. (,**0) : A geometrical model of bound

Wraith, J.M. and D. Or (+333) : Temperature e#ects onwater permittivity based on weighted averages :soil bulk dielectric permittivity measured by

the allophane analogue. Journal of Hydrology,

time domain reﬂectometry : Experimental evi--+0 : 32ῌ+*1.

dence and hypothesis development. Water Resour.

Riley, T.C., T.A. Endreny and J.D. Halfman (,**0) :Monitoring soil moisture and water table heightRes., -/ : -0+ῌ-03.

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with a low-cost data logger. Computers & Geosci-

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ences, -, : +-/ῌ+.*.

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Robinson, D.A., S.B. Jones, J.M. Wraith, D. Or and S.P.

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J. Jpn. Soc. Soil Phys.

No. +*3, p. ,1.. ,**2
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j *ῌ**ῌ ***Properties of Surface Crusts of Converted Paddy Soils
Formed under Simulated Rainfall
Hiroshi OBARA*, Tomoki TAKAHASHI** and Hisashi HOSOKAWA**** National Agricultural Research Center, Hokuriku Research center,(NARC Hokuriku) +ῌ,ῌ+ Inada, Joetu, Niigata 3.-ῌ*+3-, Japan(present : National Institute for Agro-Environmental Sciences,-ῌ+ῌ- Kannondai, Tsukuba, Ibaraki -*/ῌ20*., Japan)** NARC Hokuriku (present ; Shizuoka Prefectual Research Institute of Agriculture
and Forestry, 012ῌ+ Tomioka, Iwata, Shizuoka .-2ῌ*2*-, Japan )*** NARC Hokuriku
Abstract
Soil crusting is one of the major problems a#ecting the emergence of soybean seedlings inconverted paddy ﬁelds in some regions of Japan. To identify the converted paddy ﬁelds inwhich soybean emergence is at risk from soil crusting, we collected twenty-seven samples of
surface soils from paddy ﬁelds across Japan. Relationship among physical and chemical properties, clay mineralogy and surface crusting under simulated rainfall were studied.
In terms of morphology, most of the soil samples showed crust after exposure to a rainfall of -1
mm/h. With regard to the relationship between crust properties and soil characteristics, somecorrelations were found between the decrease in inﬁltration and the hardness and area of thecracks when crust dries.
aggregates.

The inﬁltration rates were correlated with the mean weight diameter of

The hardness indicated a rather obscure correlation between the silt contents andacid-oxalate-extractable aluminum (an indicator of Andic properties).

The cracked areas wereclearly correlated with the sand contents. With regard to clay mineralogy, in the soil samples
which showed no or trace peak for kaolinite and vermiculite and a clear peak for smectite,
hardness did not increase after drying.
Key words : soil crusts, converted paddy ﬁelds, soybean seedling emergence, physicochemical
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33


properties of soils4
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34

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

Table - Crust properties formed using a rainfall simulator4


no

#+
#,
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2345
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mm
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Correlation between crust properties4

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Fig. ,

35

Crusts formed using a rainfall simulator.

῏ῌ.
Table .

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Table / Correlation between crust properties and soil physicochemical properties4
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40

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Holder, C.B. and Brown, K.W. (+31.) : Evaluation of῍

simulated seedling emergence through rainfallῌ

induced soil crusts. Soil Sci. Soc. Amer. Proc., -2 :1*/῍1+*.

Asgedom, G.G. and Hasegawa, S. (,**/) : The e#ect ofraindrop impact and initial soil conditions on=

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Ben-Hur, M., Shainberg, D., Bakker, D. and Keren, R.

wetting and textuure e#ects on aggregate stabil-(+32/a) : E#ect of soil texture and CaCO- content

ity, seal formation, and erosion. Soil Sci. Soc. Am.

on water inﬁltration in crusted soil as related towater salinity. Irrigation Science, 0 : ,2+῍,3..

J., 02 : +33,῍+333.
Le Bissonnais Y. (+330) : Aggregate stability and as-

Ben-Hur, M., Sheinberg, I., Keren, R. and Gal, M. (+32/

sessment of soil crustability and erodibility : I.

b) : E#ect of water quality and drying on soil

Theory and methodology. European J. of Soil

crust properties. Soil Sci. Soc. Am. J., .3 : +3+῍+30.
Bennett, O.L., Ashley, D.A. and Doss, B.D. (+30.) :Science, .1 : .,/῍.-1.
Lemos, P. and Lutz, J.F. (+3/1) : Soil crusting andMethods of reducing soil crusting to increasesome factors a#ecting it. Soil Sci. Soc. Proc., ,+ :cotton seedling emergence. Agronomy J., /0 :.2/῍.3+.

+0,῍+0/.
Bresson, L.M., (+33/) : A review of physical manage-

McDonald, R.C., Isbell, R.F., Speight, J.G., Walker, J.
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land survey, Field Handbook. CSIRO, pp. +.+῍+.,,system. Research opportunities. Aust. J. Soil Res.,

Canberra Australia.

-- : +3/῍,*3.
Cattle, S., Cousin, I., Darboux, F. and Le Bissonnais, Y.
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Zealand Soils Conference, /῍3 December ,**.,

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Univ. of Sydney, Australia. CDROM, Website
www.regional.org.au/au/asssi
Chartres, C. J., Kirby, J.M. and Raupach, M. (+33*) :mahji soil. /0Rj  +33 : +1῍,,.

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crusted soil conditions. I. E#ect of crust imped-

land management. Land and Water Develop-

ance to seedling emergence. Plant and soil, 0, :ment Division Soil Resources, Management andConservation Service. pp. +0῍+1, Roma.

31῍+*/.
Rolston, D.E., Bedaiwy, M.N. and Louie, D.T. (+33+) :

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Updhyaya, S.K., Sakai, K. and Glancey, J.L. (+33/) :mineralogy e#ect on rain inﬁltration, seal forma-

Instrumentation for in-ﬁeld measurement of soil

tion and soil losses. Soil Scinece, +/,ῌ0 : .//ῌ.0,.

crust strength. Transaction of the ASAE, -2 : -3ῌ

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J. Jpn. Soc. Soil Phys.

No. +*3, p. ./῍/* ῎,**2῏Analysis of Surface Runo# in a Sloping Sandy Soil in Northeast Thailand Using Soil Water Storage Capacity
Hiromasa HAMADA*, Hiroki WATABE**, Toshitsugu MOROIZUMI***and Somsak SUKCHAN***** Japan International Research Center for Agricultural Sciences,
Owashi +ῌ+, Tsukuba, Ibaraki, -*/ῌ2020, Japan** Chugoku Shikoku Agricultural Regional Administration O$ce, Azashosakai,ῌ+, Kawabata, Itano, Tano-gun, Tokushima, 113ῌ*+*,, Japan*** Okayama University, Tsushima-naka ,ῌ+ῌ+, Okayama, 1**ῌ2/-*, Japan**** Land Development Department, ,**-/0+ PhaholyothinRd., Lardyao, Chatuchak, Bangkok, +*3**, Thailand
Abstract
In Northeast Thailand, permeable sandy soils are widely distributed. Most rainfall may inﬁltrate the ground and there may be little surface runo#. However, soil erosion caused by surface
runo# has been reported. To investigate the mechanism by which surface runo# occurs, weselected a sloping area where the top soil consisted of a permeable sandy layer overlying a very
low permeability clay layer. We deﬁned the soil water storage capacity of the sandy layer at aparticular time as the di#erence between the maximum observed water content and the observed
water content at that time. We assumed that when the amount of rainfall exceeded the soil water
storage capacity, the excess rainfall became surface runo#. As a result of monitoring of soil watercontent in the sandy soil layer over a period of one year, the total amount of runo# was estimatedto be about -*ῌ of the total rainfall and the periods for which our analysis showed that soil water
storage capacity was exceeded were followed by rises in the water level of a pond that surface
runo# ﬂowed into.
Key words : Northeast Thailand, Sandy soil, Soil water storage capacity, Sloping layered soil,
Surface runo#+.

Introduction

The Northeast Thailand region accounts for
one-third of the total area of Thailand. The
topography of the region is undulating hills,
and sandy soils occupy about 2*ῌ of the area.
Annual rainfall is +,***ῌ,,*** mm, and falls
mainly during the rainy season, May to October (Kohyama and Subhasaram, +33-). Agriculture in the region is dependent on rainfall, but
the highly variable monthly rainfall results inunstable crop yields. To use the available rainwater e#ectively, it is essential to identify the

movement of rainwater after it reaches theground surface. The permeability of the widelydistributed sandy soils in Northeast Thailand
is very high. Consequently, most rainfall may
inﬁltrate and there may be little surface runo#.
However, damaging soil erosion caused by surface runo# has been reported (Mitsuchi et al.,+320 ; Sombatpanit et al., +33/). It was di$cult
to explain the mechanism of the occurrence of
surface runo# from the viewpoint of the permeability of surface soil. Watabe et al. (,**.)
hypothesized that surface runo# would occur
after the sandy soil overlying a clay soil with



46

+*3

,**2

Fig. + Experimental site
(N : +0῍3῍ῌ E : +*,῍.2῍)very low permeability was ﬁlled with water.
However, their research has not been veriﬁed
experimentally. In this study, we measured thewater content of the sandy soil overlying avery low permeability clay soil on a hill slope
to verify the mechanism by which surface
runo# occurs.
,.

Materials and Methods,. + Study site
We selected a sloping ﬁeld covered by sandy
soil in the Nong Saeng village, about -/ km
south of Khon Kaen city. In the rainy season,
farmers in this area cultivate rice in the lowland, and sugarcane in the upland (Fig. +). The
surface slope of the sugarcane ﬁeld in ourstudy area was about - . There were two
ponds in the lower part of the sugarcane ﬁeld.
The water level in these ponds was not a#ectedby groundwater and subsurface ﬂow (Hamada
and Sukchan, ,**2), indicating that when surface runo# occurred, the water level would
increase markedly.
The soil from the surface to + m depth was
Loamy Sand (LS), 1ῌ clay, ,ῌ silt and 3+ῌ
sand. The soil below + m depth was Sandy Clay(SC), ,1ῌ clay .ῌ silt and 03ῌ sand. The

saturated hydraulic conductivity was on theorder of +*. cm/s in the LS layer and on theorder of +*0 cm/s in the SC layer (Hamada etal., ,**0). From the permeability values, we
inferred that rainwater inﬁltrated the groundand is retained in the LS layer above the SC
layer.
,. , Field investigation and analytical method
We measured soil water content (at two sites,
Site + and Site ,), rainfall, and water level in apond (P-+ : area -3* m,) (Fig. +).
Soil water content in the LS layer was measured using Proﬁle Probe (Delta-T Device, PR +/0) at depths of +*, ,*, -*, .*, 0* and +** cm atintervals of about one week between September ,*, ,**- and September ,*, ,**.. Using
these data, we estimated the soil water storage
capacity of the LS layer. The soil water storage capacity on a particular day was deﬁned as
the di#erence between the maximum recorded
volumetric water content of the LS layer (June+0, ,**.) and the measured value on that day.
We assumed that when the amount of rainfall
was less than the soil water storage capacity,
all rainfall would inﬁltrate, and when theamount of rainfall was greater than the soil
water storage capacity, the excess would become : Analysis of Surface Runo# in a Sloping Sandy Soil in Northeast Thailand Using Soil Water Storage Capacity

47

Fig. , Estimation of soil water storage capacity (at site + on April 1, ,**.)

surface runo#. The process for estimation of thesoil water storage capacity is shown in Fig. ,.
We measured water levels in the pond P-+ byusing survey instruments, GPS positioning(Sokkia, RADIANTM IS) in order to check theoccurrence of surface runo#. First, we measured the elevation of the bottom of the pond.
We then calculate the depth of water in thepond as the di#erence in the elevation between
the water surface and the bottom of the pond(error : *.*, m). The water-level measurements were recorded at intervals of one to two
weeks from March +, ,**. to September +1,,**..
Rainfall data was collected at intervals of +*minutes with a rain gauge (SEC, WeatherBucket).
-.

Results and Discussions

Figure - shows daily rainfall and calculated
soil water storage capacity in the LS layer atsite + and , (squares and triangles). The total

rainfall was +,00 mm during the period of ourinvestigation. The soil water storage capacity
was calculated at intervals of about one week.
It was therefore necessary to determine thedaily soil water storage capacity in order toestimate the daily amount of the surface
runo#. We calculated the daily soil water storage capacity by using the following equation :WnWn+Pn

Enῌ

where on day n, Wn is soil water storage capacity (Wn * indicates surface runo#), Pn is daily
rainfall, and En is daily evapotranspiration(September ,+, ,**- was day one). We assumed
that deep percolation beyond a depth of + m
was negligibly small. Daily values of E used in
Equation (+) were chosen by trial and error. We
used + mm/day from September ,+, ,**- to January +2, ,**. and as - mm/day from January+3, ,**. to September ,*, ,**., chosen so that,
Wn values (Solid line in Fig. -) would follow

48



+*3

,**2

Fig. - Daily rainfall and estimated weekly and daily soil water storage capacity

Fig. . Estimated surface runo# (Total : -1. mm)

the trend of calculated capacities using weekly
observed soil water content. Using Wn obtainedwith Equation (+), we estimated the daily surface runo# as the di#erence between the amountof rainfall and soil water storage capacity.
Our analysis results showed that the surface
runo# occurred between September ,* to October ,*, ,**-, in the middle of June, ,**., between July ,* and August ,*, and on Septem-

ber ,*, ,**. (Fig..). The total amount of runo#
during the period of our study was estimatedto be -1. mm, which was about -*ῌ of the total
rainfall (+,,00 mm). The temporal relationshipbetween daily surface runo# and variations ofwater level in the pond (Fig. /) shows that theperiods when the water level rose in the pondcoincided with periods of surface runo#, thus
validating our hypothesis that runo# occurs

 : Analysis of Surface Runo# in a Sloping Sandy Soil in Northeast Thailand Using Soil Water Storage Capacity

49

Fig. / Relationship between estimated surface runo# and depth of the pond (P-+).

when the amount of rainfall exceeds soil water
storage capacity.
..

Conclusion

This study identiﬁed the mechanism bywhich surface runo# occurs in a sloping area inNortheast Thailand, where the soil from thesurface to + m depth is LS layer and overlies avery low permeability SC layer. We deﬁned
soil water storage capacity as the di#erence
between the maximum water content we observed in the LS layer and observed values.
We assumed that when the amount of rainfall
exceeded soil water storage capacity, the excesswater became surface runo#. The periods
during which we estimated that surface runo#
occurred coincided with rises in the water levelof the pond that surface runo# ﬂowed into,
thus validating our hypothesis that runo# occurs when the amount of rainfall exceeds soil
water storage capacity.
Acknowledgement
We would like to acknowledge the usefulsuggestions for this research from Dr Shuichi
Hasegawa of Hokkaido University. We would
also like to thank Mr Chikara Ogura, from the
National Agriculture and Food Research Or-

ganization, for his assistance in our ﬁeld investigations.
Reference
Hamada, H. and Sukchan, S. (,**2) : Monitoring ofradon-,,, concentration in surface waters of
the Ban Phai subwatershed northeast Thailand using a method to concentrate radon by
air-circulation, JARQ, .,, 0-ῌ02.
Hamada, H., Moroizumi, T. Watabe, H., Srisuk K.
and Hasegawa, S. (,**0) : Soil water and groundwater in Nong Saeng, JIRCAS Working
Report, .1, pp.,1ῌ-+, Tsukuba.
Kohyama, K. and Subhasaram, T. (+33-) : Salta#ected soils in northeast Thailand, theirsalinization and amelioration. ADRC technicalpapers, No. ++, pp. +ῌ/., Khon Kaen.
Mitsuchi, M., Wichadit, W. and Jeungnijiirund, S.
(+320) : Outline of soils in the northeast plateau, Thailand, ADSC Technical papers, No.+,
pp. +ῌ2*, Khon Kaen.
Sombatpanit, S., Rose, C.W., Ciesiolka, C.A. andCoughlan, K. J. (+33/) : Soil and nutrient loss
under rozelle (Hibiscus subdari#a L. var.altissima) at Khon Kaen Thailand, Soil technology,
2 : ,-/ῌ,.+.
Watabe, H., Hamada, H., Moroizumi, T. and Hasegawa, S. (,**.) : A mechanism of surface runo#
at a sloping sandy ﬁeld in Northeast Thailand,
Proceeding of Symposium of Japan Society of
Soil Physics, +2ῌ+3, Okayama, in Japanese.

  +*3  ,**250

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J. Jpn. Soc. Soil Phys.

No. +*3, p. /+/0 ,**2
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

¯*ῌ°±²*ῌ³P´µ*Improvement of the Measurement Apparatus for Convective
Velocity of Ponded Water in Paddy Fields
Susumu HANAYAMA*, Tatsuaki KASUBUCHI* and Takeyuki ANNAKA** Faculty of Agriculture, Yamagata University, +῏,- Wakaba-machi,
Tsuruoka, Yamagata, 331῏2///, Japan
Abstract
We improved the measurement apparatus for convective velocity of ponded water in paddy
ﬁelds, proposed by Fujimaki et al. (,***).

Since the e#ect of air bubbles accumulated along thesensor on the measurement values was observed, we developed a new equipment to prevent air
bubbles from accumulating along the sensor.

Another improvement was that the power sourcesof all measurement devices in the apparatus were exchanged from AC power supplies to DC
power supplies.

This improvement allowed us to measure convective velocity of ponded waterin paddy ﬁelds without AC power supplies.

The good performance of the improved apparatus

was veriﬁed by the measurement of convective velocity of ponded water in a paddy ﬁeld.
Key words : ponded water, convective velocity, bubbles, DC power supply

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J. Jpn. Soc. Soil Phys.
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No. +*3, p. /10/ ,**2

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4 5µ*ῌ¶m6·*ῌ23¸¹*
Measuring Temporal Changes in Flooding Depths in a Rice Paddy Field
Using Time Domain Reﬂectometry
Tomotsugu YAZAKI*, Yuki SHOJI* and Kosuke NOBORIO** School of Agriculture, Meiji Univeristy, +ῐ+ῐ+ Higashimita,
Tama-ku, Kawasaki, Kanagawa ,+.ῐ2/1+, Japan
Abstract
Measurement of temporal changes in hydrological condition such as a ﬂooding depth is needed
to understand green-house gas exchange between paddy rice ﬁelds and the atmosphere. We
introduced a simple method to monitor the ﬂooding depth using time domain reﬂectometry(TDR). The results of laboratory experiments indicated that water depths measured with TDR
agreed well with those observed when the water depth was estimated assuming that the second
reﬂection of TDR pulse occurs not at the end of the rod, but at the water surface with large water
depths.

The laboratory experiments revealed that TDR provided precise enough water depths sothat ﬁeld experiments were conducted.

Water levels measured with a ,*-cm long TDR probe

agreed well with those measured with a pressure-type water gauge with a root mean square error(RMSE) of *.,2 cm.

The water levels measured by TDR, however, might be a#ected by raindrop

depositions.
Key words : TDR method, electromagnetic wave, rice paddy ﬁeld, ﬂooding depth, continuous
measurement

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!, V( ,*0!4#+ 234# +* cm, +/ cm, ,* cmTDR +4, Ksts [P\, ,- +/ cm1,+ cm, &S +, cm./ PpoP,-k, ~rz4[P\¥xcd4,
Campbell ¨]TDR ( TDR+** 5*ῒ,23

Wu4#+ K4, %& *.- cm @T +* cm

3ª

*.+ cm ­l4®S¯6`T%&5 TDR +**°$

7 L a ῌ L 5K

5z

%'4#+ * ῒ ,TDR 5D± RS,-,C'4#+ 6N, LaῌL
ῑ



89, ῏ )5 ῑ )2:;4# Lwater

&4#+< %N", TDR %:5$)%23

'²oP\pWu4,

ABCDEFGHI PCTDR ", LaῌL 

ST, ῐ )%& Lwater mX75,
Lwater-y%

:"%&`'z7{5!"|#4723 TDR 4#5z, % %W4#

567+



,

KstsWu4, j4, Hefg]v³´4, Ksts %& / J'4, K LMK %&N 7 LaῌL
54#+
< ,**1
T 2 = ,3

1=,

 > ? DOY +2- @DOY,.+ 4#+ ,**1

0 = +1

DOY+02 : µ@T( + ¶ , ·5¸¹6º456 7 +*3 8 ,**2

60

ῌFig. -TDR 



The dimension of a TDR water-depth meter installed in a rice paddy ﬁeld.

  TDR 

1/ mm !

= -- cm >?@ABCD?EF%GHI)J

9%2:(;<()%K LM=N
M=?./OP6NQ/)R῏- : S TDR  ./   L N

T 2:UL+,X

YZM=[/\]^A_ C`Q

) abSc dXe [/L M=fg0VW2:(;[Ngh(ij 45k:() [l a>@C mna ./ dXe [/ XeKCoNYZ[/\] pfgq!r K DOY,*0  +0 s /*)u; / cm v9%w

 WL cm K d z TDR 0 Lwater

0 mm xQI) R῏- y) a>@{K4N|g} +,~X 

Ky)K I *(;/a () a TDR  B SDMx/* Campbell #$ (;"CR,-X, Campbell #$ %&'() TDR+***(2:() Q/st

fgS\u;()
῎

WLLwaterLwaterrefWLref)( Lwater, ref

WLref K Q/st aa%K0

2:() DOY,*0  +0 s /*

  Lwater012) a\]() TDR ; TDR 

3 cm %Q/ Lwater  ῌ %./ 

 LaῌL 2:() Ys  KADEC-

K 

MIZU, F#$  TDR 

().* mm, != +** cm,

 ¡%K TDR ¢£K ¤¥vl ./ cm ( 2:() a

I/ £§¨¢£ RMSE

()>@$2C 
L¦* cm 0LlI/3

2CJ TDR r)u; / cm v9%w

Ypfgq!

%©()

0 mm xQI; TDR . C CNYZ[/\]()

.+ y)  ª  45 W T«¬-% c­®y.¯ No. -.-T, °Lwater+,! +* +/ ,* cm -./0123

±$²³$ %db´b2:() abgK

%2:(;ῌ " CR,-X, Campbell #$ µu; /¶·db´bR῏. av

 TDR  TDR

῍ \u;()0 L water b ©. 1¸U;<=>? : TDR @75+ AB  CDῌ.


 

Fig. .

E 
 +.* cm !"#a 0  b 2 

FGH I ῌ  +../$,*.*%

YZ8(/08

 8 0+PQ῍  [ Lwater

\T



+ : + h7iM +.* cm 9j

D7 ῍ 

[ L water

rsrtuv,- root

mean square error RMSE

wx *./+ cm *./-*.-* cm  y



RMSE

s8 ῌ 7TU TO9

. RMSE 8XM῍ !῏UT Lwater !#+O7#+
\T 

Lwater8(/U/ 

8X0+75K(/0 4῎.῎b

8X0+ Lwater 8

!j

8XUPQ Lwater 8m

n op!qN#0+M3123+7(/U/TDR

bcd_ 4῎+

¢g ef Mojid, ,**,

8]^_`aZ#£g ef ¨© Lwater    ª«#+ s8X0 ¬7i­U/ mn῍±ῑ8 +
TDR

I+¥¦ L water¶[ Lwater

LaῌL 8 + K 

TDR,-.(/0+O0+PQ ]^_`aZbcd_ ef
op!qN Lwater 8!'()*#+

,-.(/0+123+TDR 



A7zN+ {ΐ

e

.,



g

j7kl#+mn

[



e WLP e [ e WLT!4῎/ 7"#e8 ,.* cm 9j / WLTWLP P~[TDR {ΐ e
TDR

e

4῎ /

e WLP 8 +.* cm 9: /e WLT/ῐ 7j[ y
WLT 8 WLP !j

567 WLP 8 +.* cm 9: /7 WLT  WLP

8(/0

;< }῏[TU+ TDRKa? ῌ123+ ;<}῏[TU+ TDR a?



! w !.7a>?>b][ w¡ῐ L a !

#+8 8 7¤[TUU¥¦]^_^_`aZbcd_

ef!

`aZbcd_ ef8 ,ef7 T[
y6O8I+ w ®¯ °e(/0

123+ y WLP 8 +.* ῎ ,.* cm

/7,., 7i­0 ῎ ²+

WLT 8 WLP !j³´7µzK+., 7i­/ &

8XM· Lwater8mn op!qN#0} ῏ [ ++M3123+*.- cm !jTU 37;<
GHz ¸

 La

8RSTU+ VW3 ,**/ O 567 8X

WLP 8 +.*῎,.* cm

iM8

8 ,* cm

῔J7K LMNῌ  [ Lwater+* cm +/ cm ,* cm 7|[Twx *.+3 cm *.1- cm +.-0 cm  ῍ !}6§ TDR  Lwater

The relationship between manually-observed and TDR-measured water depths for di#erent
lengths of TDR rods. TDR-measured water depths Lwater were calculated (a) with Eq. (0) and (b)with Eq. (2). Dashed lines show the water depths of + cm.

 Lwater   cm

61

ῒ8X0+8y 4῎/ M3 WLP 8 +.* cm 9: /

WLT

62

89:;< = +*3 > ,**2 WLP #('?@%ABC A# WLP

D?E

 +.* cm N# IJKOP/0

R ST UVC & WLref # DOY,*0 ?

QK FGH?IJKBL?M TDR WXYZ[\]^%G?@TR% AAN#_?IJKMab RUVC cde # FG. DOY

TDR WXYfZIJK\]g + cm PTH`]

+02 ? IJK TDR fZhiP?@C\

VC WXYfZ\]^%N@% TDR )j%R)klm?

+

U

Cn?# IJK# /0?oTRIJK
pqῌM)r]s+A)tu?vN WXYfZ89JK\]w[?^%G?@C\D?FG+CAxy `C.- 

zῌ0 # TDR -./0 `C WLP  ,.* cm pN# {|}~ +.* cm .#m?/0+.* cm N WLT m?/0

 WLP 

# 

? \D? K TDR WXYfZ\]^%G?`TQ TDR

G)?+CA N@T

QU

VC
zῌ1 # a  b  TDR ῌ/

TDR   WLT  
WLP   * cm  !"#$
%  &'# + : + (')*+ ,'# +.* cm  ,.* cm )*+Fig. / The relationship between water levels
measured with TDR, WLT, and thosemeasured with a pressure-type water
gauge, WLP, in a rice paddy ﬁeld. Datafor WLP*.* cm were not shown. A
solid line shows a + : + line. Dashedlines show the water levels of + cm and
, cm.

ῌ0

 TDR ,'#  +.* cm  ,.* cm )*+

?\TR WLP-WLT -./0`C WLP  ,.* cm pN?vC WLP 
WLT # {| *./ cm  `T  S 
WLT  WLP ?+C RMSE # *.,2 cm
TDR

 WLT`T # 6? ¡C¢£¤¥¦  zῌ 2 #6Ha §¨ mm h+  / [©ª TDR b c «-./0)*+ DOY+3.  +, . -* [¬+/ . ** [¬?R TDR *./ cm p }.m?7­p®

g @v ¯°S+

?\C# ¢£¤(g +, .©H ,--./0 12# ,**1 34567 DOY )*+Fig. 0 Temporal changes in water levels measured with a pressure-type water gauge and TDR. The
horizontal axis shows the day of year (DOY) in ,**1. Dashed lines show the water levels of +cm and , cm.

&'() : TDR *+,-./

ῌῌ1 a  b 

 TDR 

63

Fig. 1 Temporal changes in (a) hourly precipitation and (b) the di#erences of water levels measured
between TDR and a pressure-type water gauge.

ῌῌ2  TDR  !" a #$ b  $ c  TDR % 

 TDR Fig. 2 An example of the TDR-water gauge noise observed on a rainy day. (a) Hourly precipitation(mm), (b) temporal changes in water levels measured every ﬁve minutes with pressure-type and
TDR water gauges, and (c) the di#erences of water depths measured between pressure-type and
TDR water gauges.

   +*3 . ,**2

64 -* /01%  2&3&"3: 3!"% 3 *./ mm  2;

45&"67"8# 9% 
<=: TDR ##>$?

@3#1%" A BCDE 

F

J? ( K@3E ) 7;

6  7"7;   TDR  LF&"K

; * ῌ 2 M  N +, O - ::  PQRBCDGH %&FSH./WLTTDR TUV01 3 45W"#XY!" DOY ,+0  DOY ,,3

WH@34?BC

DL! 8#7;  BCDGH

7" 

2Z

A: BCD %& [3\-./7]H 2   : F / J#
5J^

88 TDR TUV01

%&'I

 BCDGH %&6_37 TDR +'ISH8#* #XY!"  

$Z`&45F18&" 37 01FaE&"

FbcRdef&"K: BCD9g"67"

A :;*ῌ,#XY HY i=J^F5,&"./7"

WH,h* TUV<>*F>*j?@A BCAkFM9 lm 701##AkN+nDo#XY!"

TDR: pTQq kEFG

&"8#:7;  &rsH;  88: N

tu ILvLwxyJK6#HJL7"

+

$ LaῌL Z`&4

zY Campbell M

;~FJK&"K O; eN

BCAk

Do TDR

5F+N&8#* TDR 

TDR+**

{|}

 701W;  P45FZ`&6* Q7"8#S% 

TU+  bcRdef6# "8#

 3R ./ , -  

$%"/ῌ ῍ ῐ ῏ ῎ΐ: TDR FK F\Vῒ P WX#hj (K, YZF18

<=F[A"7 - \]^_` abc  :;( lm TDR  d Lwater :W-ef KF6   \]^g

eVdx{eh 9g"#<=eRQ ij: ef k K&"# (K d#W,Nl  8H

$Fm  noppg<= qrN

¡sW- >$FtK  2   F\V

Lwater : dp*#*:(P+ du%#*:(PW-p*, ;  &"7 - ¢vw W- £x y¤F¥;  d7"z{p*j d(P

Lwater 

8 <= N|: ¦ 4}~§¨©<=yª «<= A ¬Z. : +2,*2*,+ Z­ <

&"'( )* + +, - TDR

*"8#® %   TUV#6= B ¬Z. +312*+2-°FN2&



d

¯

F®&"8#*;    

 TDR   WLT #>$  WLp
 ,.* cm ± ,F18 

lm WLP #*: WLT # WLP :²`N l  ,.* cm ±O #*: WLT :/p %  2
 iNh  ³% Do& A (

K

q´

῔

 !"#$%"

K: TDR yFjS;  iῑJones, S.B., Wraith, J.M. and Or, D. (,**,) : Timedomain reﬂectometry measurement principles
and applications. Hydrological Processes, +0 : +.+ῌ+/-.
Hou, A.X., Chen, G.X., Wang, Z.P., van Cleemput, O.

TUV«|iand Patric, W.H. Jr. (,***) : Methane and nitrousNhW- "WH&"µ*oxide emissions from a rice ﬁeld in relation to

7"8#?; soil redox and microbiological processes. Soil

TDR #>$ F6_ lm¶:·¸*./ cm¯;7;  P   &" TDR   P>$

Science Society of America Journal, 0. : ,+2*ῌ
,+20.

RMSE : *.,2

Mojid, M., Toride, N. and Cho, H. (,**,) : The e#ect of

cm 7- W,Nl  TDR  $:@heterogeneous soil-water distribution on the

34BCD"8#7- 3701 

TDR measurement of soil-water content.  : TDR 

! 3* : ++ῌ+3.

65

Schaap, M.G., Robinson, D.A., Friedman, S.P. andNadler, A., Ravehb, E., Yermiyahub, U. and Green, S.

Lazar, A. (,**-) : Measurement and modeling ofR. (,**-) : Evaluation of TDR use to monitor

the TDR signal propagation through layered di-water content in stem of lemon trees and soil andelectric media. Soil Science Society of America

their response to water stress. Soil Science Society of America Journal, 01 : .-1ῌ..2.

Journal, 01 : +++-ῌ++,+.
Tang, L., Tao, X. and Choy, C.-l. (,**+) : Possibility ofNoborio, K. (,**+) : Measurement of soil water con-using a coaxial cable as a distributed strain

tent and electrical conductivity by time domain

sensor by time domain reﬂectometry. Smart Ma-

reﬂectometry : a review. Computers and Electronics in Agriculture, -+ : ,+-ῌ,-1.

"#$% ,**- : &' TDR () *+,-ῌ.
-/0

terials and Structures, +* : ,,+ῌ,,2.
Thomsen, A., Hansen, B. and Schelde, K. (,***) : Ap-*+ ! 3- : /1ῌ0/.

plication of TDR to water level measurement.
Journal of Hydrology, ,-0 : ,/,ῌ,/2.

"#$% ῌ 12345 ῌ 6789 ῌ 8:; ,**/ :Topp, G.C., Davis, J.L. and Annan, A.P. (+32*) : Elec-,*GHz-TDR <=>?@ABCDEFG H

tromagnetic determination of soil water content :IJK .. : 31ῌ+*+.

Measurements in coaxial transmission lines. Water

Pepin, S., Livingston, N. J. and Hook, W. R. (+33/) :Resources Research, +0 : /1.ῌ/2,.

Temparature-dependent measurement error in

Weast, R.C. (ed.). (+320) : Handbook of chemistry andtime domain reﬂectmetry determination of soil

physics. pp.E/+ῌE/-. 01th ed. CRC Press. Boca

water. Soil Science Society of America Journal,

Raton, FL.

/3 : -2ῌ.-.

῍ῌLMNOPQRS>TUV WXYZ[\X] ^_V time
domain reﬂectometry TDR >)]` abc>Ud>efgA Mh&ijO

klmlXnopq TDR rns_gAV Ytu]vu&v:wg
TDR >)]xyY_uzvY{|kxA }~jO Yx !YkxA ,* cm q TDR nop>?@A TDR ccV c
v root mean square error RMSE *.,2 cm _:wgA : ,**1  +*  ,.  : ,**2  .  -*  !
J. Jpn. Soc. Soil Phys.

No. +*3, p. 011. ,**2


­²³*ῌ´µ¶**

Error Correction Method for Hydrometer Analysis in Test Method
for Particle Size Distribution of Soils
Yasuaki KOMIYA* and Toshiya SHINJO*** Faculty of Agriculture, University of the Ryukyus, Nishihara, Okinawa, 3*-ῌ*,+-, Japan** Subtropical biomass research center, Nishihara, Okinawa, 3*-ῌ*,+-, Japan
Abstract
In test method for particle size distribution of soils, sieve analysis result and hydrometer
analysis result may not be skillfully connected. It is said that in hydrometer analysis, much error
arises from many causes, and it brings about the error for the values of percent ﬁner by mass andparticle size calculated using Stokes’ law. This fact was estimated by the trial, and instrumental
error of hydrometer, density error of the water, viscosity coe$cient error of the water was
clariﬁed. Hydrometer analysis result was corrected using these.

It was conﬁrmed that thecorrected hydrometer analysis result agrees almost with the sieve analysis result using ./ mmsieve, -, mm sieve and ,* mm sieve. Then, as convenient method, the method for moving particle
size curve by hydrometer analysis parallel in the vertical direction was proposed so that thepercent ﬁner by mass of -, mm particle size by the hydrometer analysis may agree with thepercent ﬁner by mass of -, mm particle size by the sieve analysis, and the result was good.
Key words : test method for particle size distribution, hydrometer analysis, error, -, mm sieve

6;NF@KOPQCRS+,- TUBC+Y+ZWK2["#Q*\6^1Q*_ `BTaWbW6cQ!d12345

6789:*% ; <=>?

HVWX

X>*T]D+*, ]@] ef!VWGCg=hN eSiKOPQ*@2ABCDEFG "#HIJKLMFCD+*,

!"#KSjDkNFC*, JIS A +,*. .!"2 JIS lmn='(oT `BK# - =2 pX *.*1/ mm qrsKtQ*

u+Dvw] pxyz{|} 6~]

)*+nTCqKtQ*lmn6=>*, ;E JIS !"#]Dpxyz{61Q*, lmn=2 Bg

C lmn=2!iX8BCD+*X l

21 +,K}B

g;oKSjD'(X] pxyz{)*mnKtQ*5"# 2}T=+nTlmnXigVW];+TX>>? =2$%&*, ZW  /  ,***0 K2 .*.*1/

lmn0 Ku+Dvw]D+*,mm O=z{X*, C2

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*-ῌ*,+ : !"# $%&  '( -, mm )*+ +

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68

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A&34

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HIJ K r 1L<&IJM;<3NO h & rw 1 JIS 41P =" GQ RS

T3UV;<1B2W  rs 1 JIS 41X
Y

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_8  `!&NO ;<1ab4?
 Pῌ+ 
'#$% (!

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ms rsrw
῎rsrwrs+**"#$%&

d )Fig. + Combination of sieve test result andhydrometer result observed in particle
size distribution curve

rw
r s
d ῌh
῎


,῍ h
rsrwrw
rsrsrw῏
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< ;< e"f #g;<  ;<"#$& '#$ hi1jῑ+ k@8 W .

 ;<n opqr3%?   b 1 ! "UOG1&s P d r h rw rs & <45 Z ;<45  lm/0

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,+ 

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1  a8  '#$3! "#$

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



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

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69

'(Table + Dimension of hydrometer

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No

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1+-A
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223-B
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*4.1/
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*4.//

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++4**
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++41+
++42,

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V cm-+/ 0,1 d-/43,-.42,,.+4+01-.43,+--42,,--41//+4**,++4**+1+4***,+4**+++4**+*+4**+3342,
34/3343340/
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F ?4&@2A*BC >* 6

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C\=$ ]$C

^>NKL_]$3<= >[9 ]$C`a3:;b`a >* BP3cd  @3A
H  L *.33/ 68 +.*/ [ #$Cefgh_*3ihef #$2_E jk3

ῌ, 

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Fig. , hydrometer*BC2?Oq"[PN blG2r[*K3]$ #$C1AKop3r[*2
V : d, si./ cm 

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v+ : vw-_*./ cm-

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|AONl}2~8PN *V

d : {.

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A* +

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B>D? P -. +303 6 3/2 B-

3< <EN

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0,-6¡NCGC,4`a2W῍ L_ 3 
&a¤ F1yz& C

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70

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Relationship between value of hydrometer and water temperature in distilled waterῌῌ.
Fig. .



Relationship between scale and instrumental error of hydrometer'()*+,-./0 12345678/.9:;<=>?@AB'( 3.+ g ABCB>?@AB

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Fig. 0Relationship between density of waterand dissolution quantity of dispersing
agent

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71

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Relationship between viscosity coe$cientof water and dissolution quantity of dispersing agent

789: ,* ;

Table , Properties of saturated aqueous solution of dispersing agent at ,*

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Measuring example of soil particle densityof respective grain diameter*b-12R

12*b-md12*b-R T 12V34O-UR
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

72

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Comparison of soil particle size distribution curve modiﬁed by , error correction methods

!"#$%&!'()

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Comparison of clay fraction content
modiﬁed by , error correction methods

73

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Fig. +*

Comparison of content of particle of+.. mm particle size or less by pipettemethod and hydrometer method

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J. Jpn. Soc. Soil Phys.
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L.A. Richards 

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Reviewing classical studies in soil physics“Capillary conduction of liquids through porous mediums”
By L.A. Richards
Physics, + : -+2ῌ--- (+3-+)
Kosuke NOBORIO** School of Agriculture, Meiji University, +ῌ+ῌ+ Higashimita, Tama-ku, Kawasaki, ,+.ῌ2/1+
Key words : water movement, soil water content, matric potential, hydraulic conductivity, hysterisis+33-  

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²@ Z7[/s =%+*!*&*+* RichardsCampbell, G.S. (+32/) : Introduction to soil physics
with BASIC. Elsevier Pub., New York.
Celia, M.A., Bouloutas, E.T. and Zarba, R.L.(+33*) : A¢@

general mass-conservative numerical solution

K#AMEA  yE

for the unsaturated ﬂow equation. Water Resour.

>Y?@=%Z7[³+ y & K,- 4e6a4@AEg+

Klute, A. (+3/,) : A numerical method for solving the,- 4e6a4 

ﬂow equation for water in unsaturated materi-*  y & K

/n£G!*& ´Q (   µ 
+ y & q / y & K

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4e6a4

@A(& / Richards @[O+A Philip, +31.

¶*·n!¸jals. Soil Sci., 1- : +*/ῌ++0.
Narasimhan, T.N. (,**1) : Central ideas of Buckingham (+3*1) : century later. Vadose Zone J., 0 :021ῌ03-.
Nimmo, J.R. and Landa, E.R. (,**/) : The soil physics-    Res., ,0 : +.2-ῌ+.30.

contributions of Edgar Buckingham. Soil Sci.

"zASoc. Am. J., 03 : -,2ῌ-.,.

: L.A. Richards 

Or, D. (,**+) : Who invented the tensiometer? Soil Sci.
Soc. Am J., 0/ : +ῌ-.
Philip, J.R. (+31.) : Fifty years progress in soil physics. Geoderma, +, : ,0/ῌ,2*.
Richards, L.A. (+3,2) : The usefulness of capillary potential to soil moisture and plant investigation.
J. Agric. Res., -1 : 1+3ῌ1.,.

79

Richards, L.A. (+3-+) : Capillary conduction of liquids
through porous mediums. Physics, + : -+2ῌ---.
Richards, L.A. (ed.) (+3/.) : Diagnosis and improvement of saline and alkali soils. Handbook 0*.
USDA, ARS.
 : ,**2  .  +.  : ,**2  0  +0 ῒ ΐ ῏
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++0ῌ**++ OPQª«S¬­® 1+,+0/¡/Journal of the Japanese Societyof
Soil Physics
July ῍ῌῌ῎

No. +*3
Contents

Foreword ῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌI. YAMADAῌ +Original Papers
Soil Environment Monitoring by Multi-frequency Electromagnetic Sounding῎῎῎῎῎῎῎῎῎῎῎῎Y. HIRAI, Y. MORI, H. SOMURA, N. EGUSA and T. MORISAWA῎ Calibration of Temperature Dependence of a Dielectric Probe῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎T. SAITO, H. FUJIMAKI and H. YASUDA῎+/
Properties of Surface Crusts of Converted Paddy Soils Formed under Simulated
Rainfall ῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎H. OBARA, T. TAKAHASHI and H. HOSOKAWA῎,1
Notes
Analysis of Surface Runo# in a Sloping Sandy Soil in Northeast Thailand Using Soil
Water Storage Capacity ῎῎῎H. HAMADA, H. WATABE, T. MOROIZUMI and S. SUKCHAN῎./
Improvement of the Measurement Apparatus for Convective Velocity of Pounded
Water in Paddy Fields ῎῎῎῎῎῎῎῎S. HANAYAMA, T. KASUBUCHI and T. ANNAKA῎/+
Measuring Temporal Changes in Flooding Depths in a Rice Paddy Field Using Time
Domain Reﬂectometry ῎῎῎῎῎῎῎῎῎῎῎῎T. YAZAKI, Y. SHOJI and K. NOBORIO῎/1Error Correction Method for Hydrometer Analysis in Test Method for Particle Size
Distribution of Soils ῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎Y. KOMIYA and T. SHINJO῎01
Lectures
Reading of Classical Study Series“Capillary conduction of liquids through porous mediums” By L. A. Richards῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎K. NOBORIO῎1/
Readers’ column ῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌM. MIZOGUCHIῌ2+
Announcements ῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌῌ2Editor’s Postscript ῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎῎2/Japanese Society of Soil Physics
Department of Environmental Sciences
Faculty of Agriculture, Saga University+ Honjo-machi, Saga, 2.*ῌ2/*, Japan