ROCZNIKI GLEBOZNAWCZE, T. X X X II, NR 3, W ARSZA W A 1981
ZY G M U N T BRO G O W SK I, A D A M M A ZU RËK
DIFFERENTIATION'OF CLAY MINERALS IN PARTICULAR MECHANICAL FRACTIONS OF S O IL 1
D ep a rtm en t of S o il S cien ce, A g ricu ltu ra l U n iv e r sity at W arsaw
IN T R O D U C TIO N
It is w ell-know n th a t clay m inerals constitute one of m ain sorbents in soils. In this connection there is a great interest in the w orld lite ratu re in the qualitative composition of clay m inerals [1, 4, 5, 8, 12J, their form ation processes [6, 9] and m ethodical investigations concerning their determ ination [3, 7, 10, 11]. In recent years greater attention is paid to the possibility of occurrence of m inerals not only in the clay fraction of soils, b u t also in the particles of greater diam eter [2, 10].
In the present investigations the qualitative composition of clay m inerals in m echanical fractions of < 20 \im separated from leached brown soil developed from sedim ents of the old accum ulation terrace of the Vistula river in the environs of the K azuń locality near Modlin was studied.
M A TE R IA L A N D M ETH O D S
Soil m aterial taken from 8 genetic horizons of the profile was divided into mechanical particles by means of repeated separation by the A tte- b erg’s method. Soil was boiled several times and m ixed at use of the ro tary electronic m ixer, w ithout any pepticizing compounds. This operat
ion was repeated as m any times as the clay particles of < 2 jim and subsequent ones were totally elim inated off soil. The quantitative share and diam eters of the fractions separated are presented in Table 1.
The subject of roentgenographic exam inations were the fractions of < 2 \im as well as those of 2-5, 5—10 and 10-20 jutm in diam eter. The
1 T his w ork has been fin anced by the D epartm ent of A grophysics, P olish A cad em y of S cien ces, in L ublin.
T a b b 1 Feme p r o p e r t i e s and g r a n u l a t i o n o f n o i l G e n e tic h o riz o n S am pling d e p th cm pu* O rganic c a rb o n p e r c e n t* *
Per c e n t o f m ech an ical p a r t i c l e s o f mm in d ia xjtx li?0 KC1 1 -0 .5 0 .5 - 0 .2 5 0 .2 5 - 0 .1 0 .1 - 0 .0 5 0 .0 5 -- 0 .0 2 0 .0 2 * - 0 .0 1 1 о in *— о о • • о О 1 0 .0 0 5 --0 .0 0 2 <£0.002 A1 5-30 ь.о 4 .0 0 .7 0 1 .0 7 .1 3 3 .2 1 3.2 18 .0 6 .7 4 .3 3 .5 1 3 .0 /& / 30-50 5 .4 4 .1 0 . ?B 1.1 6 . 3 3 4 .9 1 3 .3 1 8 .9 6 .5 3.1 3 .5 12 .4 /в»/ 50-70 5 .6 4 .1 0 .1 9 0 .5 3.Q 2 7 .7 13.0 15.6 6 .2 3.4 4.1 2 5 .7 /ь//с 7 0 -<Ю 5 .7 4 .2 0 .2 0 0 .2 1 .0 30 .6 34 .8 11.6 2 .1 2 .3 1.6 15.8 с 90-120 5 .7 4 .2 0 .1 2 0 .2 2 .8 4 8 .7 14.6 1 4 .3 2 .7 1 .8 1.4 1 3 .5 °1 120-145 5 .6 4 .3 0 .0 9 0 .2 5 .0 4 0 .0 1 6 .3 18.4 3 .1 1 .9 2 .4 1 2 .7 с 145-165 6 .4 5 .5 0 .0 3 0 .3 2 0 .2 46 .4 11 .0 6 .7 1 0 .0 0 .6 1 .0 3.8 D1 180-200 6 .9 6 .1 0 .0 2 0 .2 2 6.1 5 2 .6 10 .2 4 .6 0 .8 0 .5 о . ь 4 .4
x - pH was d e te rm in e d by th e e l e c t r o m e t r i c m ethod a t u se o f a g la e a electro d e* ** - O rg an ic c arb o n was d e te rm in e d by th e V .T y u r in 's m ethod
*** - D eterm in ed by th e A t t e r b e r g 's m ethod by means o f re p e a t e d s e d im e n ta tio n , b o i l i n g and m e c h a n ic a l m ix in g , w ith o u t ur.y p e p t i c i z i n g compounds
1 2. ß r o g o w sk i, A . Maz ure k
Clay minerals in soil mechanical fractions 195
exam inations were perform ed on the TUR-M-62 apparatus while ap plying the Со К radiation at the iron filter, voltage of 34 KV and am perage of 10-14 mA.
The subject of exam inations under infrared rays were only the fract ions of < 2 ц т . The VR-10 C. Zeiss-Jena spectrophotom eter was applied in the examinations. Samples for exam inations were prepared in the form of presented tablets w ith potassium bromide. The spectres under infrared rays were registered w ithin the range of 400-4000 cm“ 1.
D IS C U S S IO N OF R ESU L TS
T h e f r a c t i o n o f < 2\im. In p artucular genetic horizons of the soil investigated this fraction show a sim ilar m ineral composition (Figs 1, 2, 3). Smectites (14 Â), kaolinite (7.13 and 3.57 Â), quartz (4.23 À) and in less am ount illite (9.9 À) prevail in it. It can be presum ed from the intensity of 4.23 Â reflexes th a t the am ount of quartz in the colloidal particles would be gradually decreasing w ith the soil profile depth.
Fig. 1. Difractograms of the fractions of < 2 |лт separated from different genetic horizons of soil
F ig. 2. D ifra cto g ra m s of th e fra ctio n s of < 2 ц т at th eir d iffe r e n t p rep aration
Sim ilar in the case w ith the kaolinite content. On the other hand, the am ount of m inerals w ith interlayer spacings am ounting to about 14 A would increase w ith the profile depth (Fig. 1). The 14 Â effects of these m inerals are relatively wide, particularly in the horizons laying w ithin the depth of 30-120 cm (Fig. 1). Under the effect of heating in 300°C a collapse of smectites is taking place and their interlayer spacings are decreasing to about 10 A (Fig. 2). Only in the horizon of 5-30 cm the collapse occurred only at 400°C. Probably in this case the effect of organic compounds or exchangeable cations situated in the interleyer spaces would occur (Fig. 3).
All genetic horizons analyzed contain clay m inerals of the illite group, of which the effects of about 9.9 Â can bear evidence. These
Clay minerals in soil mechanical fractions 1 9 7
F ig. 3. S p ectres of absorption in in fra red s of th e fra ctio n s of < 2 ц т separated from d iffe r e n t g en etic h orizons of soil
effects are small (low). The presence of kaolinites was detected on the bassis of the 7.13 and 3.57 Â reflexes and of ignition of samples in the tem perature of 550-580°C, in which kaolinite disintegrates and in this connection roentgen reflexes vanish from this m ineral [21]. The presence of chlorites or verm icullites in clay fractions of some horizons (5-30, 30-50 and 120-145 cm) can possibly be proved by the reflex of about 4.70 Â, b ut it is not cleare evidenced corroborated by low-angle reflexes.
Spectres under infrared rays confirm the predominance of m inerals
of the 2 : 1 type over kaolinite (Fig. 3). Among non-clay m inerals in
these particles quartz occurs (4.23 Â and in the infrared spectres 775 and 794 cm*"1). The infrared spectres w ere made for particles w ithout and w ith preparation by means of the hydrogen peroxide solution. The
hydrogen peroxide solution are omited. In upper soil layers the presence of absorption spectra originating from humus substances (595, 677, 1390 and 2940 cm“ 1) was found.
T h f r a c t i o n s o f > 2 цт. Parageneses of m inerals in the fract ions coarser than 2 jim are distinctly differentiated. Along w ith diam eter grow th of mechanical particles a system atic increase of the content of quartz and feldspars is observed. A little differentiated m ineral com position has the fraction of 2-5 \xm from the A 1 horizon (Fig. 4). In this horizon, beside quartz and feldspars, an traces am ount of hydro micas occurs (4.93 and 9.9À) (Fig. 5).
In the horizons of 70-90 and 120-145 cm the am ount of hydromicas in the fraction of 2-5 \im is distinctly higher (Fig. 4). In coarser
fract-Fig. 4. Difractograms of the fraction of 5-2 [im separated from different genetic horizons of soil
Clay minerals in soil mechanical fractions 199
F ig. 5. D ifractogram s of d iffe r e n t m ech an ical fra ctio n s from th e А г horizon. 5-30 cm
ions separated from these horizons (Figs 6 and 7) a certain adm ixture,
most probably of chlorites — verm icullites is vissible (14.0, 4.7, 7.1 and
3.57 A). M inerals of this group (chlorite — verm icullite) respond readily
to ethylenglycol (Fig. 8) and collapse under heating to about 10 A.
The fraction of 2-5 \im separated from the horizon of 70-90 cm contained m ostly m inerals w ith the wide m axim um w ithin the range
of 10-14 A (Figs 4 and 6). These m inerals collapse under ignition and
show an wide reflex of 10.0-8.4 A after glycolation (Fig. 8). That proves
a prevalence of smectite and illite stru k tu res in this fraction.
Among the set of clay m inerals in the m echanical fractions invest igated a predom inant role play smetites, less of illites and kaolinites. T hat is confirm ed by the data concerning the sorption capacity of the
fractions investigated (Table 2). These data comprise an unfull sorption
capacity as they concern only the sum of exchangeable cations (C a+ M g + + K + N a), not comprising exchangeable or hydrolytic hydrogen. Sorption capacity of the m echanical fractions investigated depends also on hum us compounds (Table 2), w hat is visible in the fractions separated from the A t horizon.
F ig. 6. D ifraotogram s of d ifferen t m echanical fractions from the (В) С horizon, 70-90' cm
of- these fractions distinctly proves a prevalence of m inerals of the 2 : 1 type over those of the 1 :1 stru ctu re (Tables 2 and 3). A relative d istri bution- of m inerals in mechanical fractions separated from different horizons and layers d i soil prove tentative data quoted in Table 3.- The vertical differentiation in the soil profile among secondary clay, m inerals is little. It proves ä w eak effect of the' soil-forming processes in still relatively young (about 10 500 years) soil m aterial.
C O N C LU SIO N
On the basis of the present detailed investigations the following conclusions can be draw n :
1. The clay fraction of all genetic horizons shows a predominance of smectites. Illite and kaolinite show a less precentage in the m ineral composition. A lack of any distinct differentiation of the m ineral com position of the clay fraction in the whole soil profile proves a weak effect of soil-forming processes on a relatively young soil m aterial.
Clay minerals in soil mechanical fractions 201
F ig. 7. D ifractogram s of d iffe r e n t m ech a n ica l fra ctio n s from th e С horizon. 120-145 cm
low, even in the colloidal fraction. In spite of that, the sorption capacity greater differentiation in the m ineral composition. It is observed p ar ticularly distinctly in deeper soil layers.
3. The results obtained allow to presume th a t there would be a
great probability of occurrence of clay m inerals also in the fraction of 2 - 2 0 \im.
to
T a b l e 2 The c o n tc n t o f o rg a n ic c arb o n and humus compounds and th e s o r p t i o n c a p a c ity
i n r e l a t i o n to e x ch a n g e a b le b a a e s in m e c h a n ic a l f r a c t i o n s
G e n e tic Sam plingd e p th O rg a n ic carbon p u r c e n t in m e c h a n ic a l f r a c t i o n s * Sum o f b a s e s /Ca»-Mg+K+Na/ in m .e. p e r i n th e f r a c t i o n s o f:* * 100 g
h o riz o n cm 2 0-10
/лп 10-5jjia 5 -?pm < 2 jam 20-10/am 10-5urn 5-2 <r 2 /ш
A1 5-30 1.35 2 ,4 0 3 .05 3.28 9.31 21.41 20 .0 6 167.48 /В / 30-50 0 .3 5 0 .6 5 0 .6 3 1.10 4 .5 3 Û.-22 21 .0 0 5 9 .3 0 /В * / 5 0-70 0 .0 5 0 ,1 0 0 .3 5 0 .6 0 5 .4 6 9.Э0 2 5 .1 9 51 .4 6 /В //С 70 -9 0 0 .4 2 0 .5 7 0 .5 0 0 .7 7 9 .9 5 1 2.62 13.39 4 2 .4 9 с 9 0-120 0 .2 0 0 .3 3 0 .4 4 0 .6 0 4 .6 2 9 .16 19.92 4 2 .5 5 C1 120-145 0 .1 2 0* 34 0 .3 6 0 .4 4 4 .3 0 10.50 1 7.76 4 4 .6 0 » 145-165 0 .1 5 0 .3 5 0 .6 0 0 .4 4 6 .0 2 12.08 23.0 6 5 4 .6 6 D1 180-200 0 . 1 6 0 .3 3 0 .5 4 0 .5 4 7 .0 0 13.04 2 2 .9 7 56 .7 5 Mean - 0 .3 5 0 .6 3 0 .8 2 0 .9 7 6 .4 0 12 .1 2 ! 1
j
2 0.42 64.91x - O rg a n ic c arb o n was d e te rm in e d by th e V .T yU Tln'a method
** - E xch an g eab le c a t i o n s were d e te rm in e d in th e 1 N ammonium a c e t a t e e x t r a c t
I. B r o g o w sk i, Л . M a z u r e k
C lay m in erals in so il m ech an ical fraction s 203
T a b l e 3 Relative occurrence of clay minerals Is mechanical fractions
Genetic Sampling depth Means for mechanical fractions - m a
horizon on < 2 2-5 5-10 10-20
A1 5-30 ++OOXX.• OCX... OX.,, 0 , . ,
/В/ 30-50 ++OOXX.. oox... OX.., 0 . . .
/В* / 50-70 ++ООП . . +OCX... ox,.. OX...
/В/ /С 70-90 +++OXXX.. ++OOX., ++OX., +OX...
с 90-120 +++CX.' OOX. • o x . . . ox...
C 1 120-145 ♦-»■•vox. 4000X.•• OX.*. +COX...
D 145-165 +++OX. +OOX... OX... OOX...
D1 130-200 +++OX. +OOX... o x . . . OOX...
+ - s m e c t it e m in e r a ls о - i l l i t e m in e r a ls X - k a o l i n i t e m in e r a ls
- o t h e r s / q u a r t z , f e l d s p a r « / + - o c c u r r in g in l i t t l e num bers
- o c c u r r in g in medium num bers +++ - o c c u r r in g in g r e a t numbers
F ig. 8. D ifra cto g ra m s o f fra ctio n s of d iffe r e n t d ia m eter a t th eir d iffe r e n t prep aration fro m th e (В) С horizon, 70-90 cm
R EFEREN CES
{1] C h o d a k T. : In v e stig a tio n s on p rop erties and m in erai com p osition of soils d ev elo p ed from lo ess in th e L ow er S ile sia region. Zesz. nauk. AR W rocław , 1980, 21, 49.
i [ 2 ] E s w a r a n H., W ong C haw B in : A stu d y of deep w e a th e r in g p ro file on
g ra n ite in p en in su la r M alaysia. II. M in eralogy of th e cla y , silts and fr a c t ions. S o il S ei. Journ. Soc. o f A m er. 42, 1978, 1, 149-153.
[3] K ę p k a M. : P r e lim in a r y in v e s tig a tio n s of th e m in era l fra ctio n o f < 0 .0 0 2 m m of p od zolic and b row n soil. R ocz. gleb ozn . 1962, 161-171.
[4] K o m o r n i c k i T., A d a m c z y k В., J a k u b i e c J., К u b i s z J., O l e k - s y n o w a K. , T o k a j J. : C lay m in era is o f so ils d ev elo p ed from upper T ria ssic rocks in th e T atra m ou n tain s. R ocz. gleb ozn . 11, 1962, 161-172. [ 5 ] K o m o r n i c k i T. : O rganic origin of cla y m in erals. R ocz. glebozn., a n n ex
to th e vol. 7, 1958, 201-212.
[6] K o n e c k a - B e t l e y K. : A contribution to th e recogn ition of clay m inerals in so ils d ev elo p ed from lo esses. R ocz. gleb ozn . 16, 1966, 2,. 413-439.
[7] O l e k s y n o w a K., Z a s o ń s k i S. : E ffect of p relim in a ry p rep aration w ith h yd rogen perosid e on d iffe r e n tia tin g cu rv es of cla y m in erals. Rocz. glebozn. 19, 1968, 279-289.
[8] P a V e 1 L., U z i a к S. : C lay m inerals of soils d evelop ed from loess and silt fo rm a tio n s of the w ater origin. R ocz. gleb ozn . a n n e x to th e v ol. 9, 1960, 160-163. [9] P r u s i n k i e w i c z Z., G o r b u n o v N. I., G r a d u s o v B. P. : F orm ation
of cla y m in era ls in p od zolic so ils d ev elo p ed from co a sta l dune sands of d if feren t age. Rocz. gleb ozn . 14, 1964, 2, 375-378.
[10] S t o c h L. : C lay m in erals. W ydaw . G eologiczn e, W arszaw a 1974, 503. [11] S t o c h L., S i k o r a W. : In v e stig a tio n s on the gra n u la tio n of cla y -minerals in
soils and loam s. Rocz. glebozn. 19, 1968, 291-298.
[12] U z i a к S. : M in eralogie com p osition of the c la y fra ctio n of soils d ev elo p ed from silty fo rm a tio n s o f d iffern t origin. R ocz. gleb ozn . 14, 19/64, 2, 367-374.
Z . BROGOWSKI, A. MAZUREK
ZRÓ ŻN IC O W A NIE M IN ERA ŁÓ W IL A ST Y C H W R ÓŻNYCH FR A K C JA C H M ECH A N IC ZN Y C H GLEB 1
In sty tu t G leb o zn a w stw a S G G W -A R w W arszaw ie
S t r e s z c z e n i e
M in erały ila ste oznaczono w o d d zieln y ch fra k cja ch m ech a n iczn y ch o średnicy: < 2 [im, 2-5 [im, 5-10 um i 10-20 |.im, w yd zielo n y ch z gleb y brunatnej w y łu g o w a nej w y tw o rzo n ej z utw oru sta ro a lu w ia ln g o z o k o licy M odlina.
M in erały oznaczono ap aratem ren tg en a T U R -M -62 stosu jąc p ro m ien io w a n ie Co K, n a p ięcie 34 KW i n a tężen ie 10— 14 mV.
W w y n ik u przep row ad zon ych badań stw ierd zon o, że w w ierzch n ic h p oziom ach badanej g leb y w ię k sz y u d zia ł w e fra k cja ch p o sia d a ją m in era ły illito w o -k a o li- to w e , n a to m ia st w g łęb szych poziom ach m in era ły illito w o -sm e k ty to w e . N a le ż y jedy nak p od k reślić, że k a o lin it i h y d ro ły szczy k i sta n o w ią w ię k sz y u d ział w e fr a k
-Clay minerals in soil mechanical fractions 205
cjach gru b szych , n a to m ia st w e fr a k c ji ila ste j d om in u jącą rolę o d g ry w a ją sm ek - ty ty . F rak cja ila sta za w iera rów n ież zn aczn e ilo śc i k w a rcu szczeg ó ln ie w p ozio m ie A v
P ro f. dr Z y g m u n t B r o g o w s k i I n s t y t u t G l e b o z n a w c z y A R W a r sz a w a , R a k o w i e c k a 26
