ACTA GGM DEBRECINA Geology, Geomo phology, Physical Geog aphy Se ies DEBRECEN Vol. 3, 9–14 2008
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Mine alogical composi ion o gene ic ho izons o c us y meadow solone z soil p o ile om
Püspökladány based on X- ay di ac ion and he mal analysis
Püspökladányi ké ges é i szolonyec szel ény gene ikai szin jeinek ás ányi össze é ele ön gendi akciós és e mikus
analízis alapján
† Gyula Szö 1 – É a Balázs 2 – Tibo No ák 3 – Pé e Ko ács-Pál y 4– Pé e Kónya 4
1Depa men o Mine alogy and Geology, Uni e si y o Deb ecen; 4032, Deb ecen, Egye em é 1.
2BIOGÁL-TEVA, Deb ecen; 4042 Deb ecen, Pallagi ú 13.
3Depa men o Landscape P o ec ion and En i onmen al Geog aphy, Uni e si y o Deb ecen; 4032, Deb ecen, Egye em é 1.
4X- ay di ac ion Labo a o y, Geological Ins i u e o Hunga y (GIH); 1143, Budapes , S e ánia ú 13.
Abs ac – A ypical solone z soil p o ile, cha ac e is ic o he Ho obágy egion (Eas e n Hunga y) was chosen in Ágo a-pusz a,
Püspökladány, o s udy he mine al dis ibu ion in gene ic soil ho izons. The analyses we e ca ied ou o ge ing da a abou mine al
composi ion o he egion’s mos ypical soil ype, and compa e i wi h solone z p o iles om o he egions o he G ea Hunga ian Plain.
On he o he hands i was aimed o poin on he possible mine al ans o ma ion p ocesses causing he s ong di e en ia ion be ween
gene ic ho izons o he p o ile. The analysis es ablished ha he mine al composi ion o he pa en ock is e y simila o ha o o he
Hunga ian solone z soils. The dominan mine al is qua z (44%). Second equen mine al g oup a e clay mine als (35%), hei p opo ion
is highe han he p opo ion o he clay size ac ion de e mined by he sedimen a ion me hod (19.5%), he e o e one pa o hem alls
in he g ain-size class >2µm. Main componen s a e also micas (musco i e+illi e) (14%) and plagioclase (9%). As a consequence o soil
o ma ion, he uppe ho izons show signi ican de ia ion om he mine al composi ion o he pa en ock. In ho izon “A” p opo ion o
qua z eaches 59%. A highe amoun o clay mine als (45%) is cha ac e is ic o he „B” ho izon as a esul o clay p oduc ion and
illu ia ion. As inal esidual p oduc s o mine al deg ada ion goe hi e, hema i e, gypsum and amo phous componen s occu in lesse
amoun s, wi hou signi ican di e ences in hei e ical dis ibu ion.
Össze oglalás – A Ho obágy e üle én jellegze es, ipikus ké ges é i szolonyec alajszel ény álasz o unk ki Ágo a-pusz án a a a cél a,
hogy a alaj ás ányos össze é elének gene ikai alajszin ek közö i különbségei meg izsgáljuk. A izsgála ok észben a a i ányul ak, hogy a
izsgál e üle alajai ás ányi össze é el ekin e ében más hazai szolonyec szel ények ada ai al összehasonlí hassuk, más ész pedig az
e sen di e enciál szolonyec szel ény különböz gene ikai szin jei közö el é elezhe ás ányá alakulások olyama ai ól nye jünk
in o mációka . A izsgála ok ük ében a alajképz k ze ás ányi össze é ele nagyon hasonló más hazai szolonyec alajú e üle ekéhez.
U alkodó ás ány a k a c (44%). Emelle az agyagás ányok jelenlé e számo e (35%), mennyiségük meghaladja az iszapolással
megha á ozo agyag akció mennyiségé (19,5%), ehá egy észük a >2µm nagyság endbe a ozik. Az alapk ze jellegze es ás ányai még
a csillámok (muszko i +illi ) (14%) és a plagioklászok (9%). A alajképz dés kö e kez ében kialakul különbségek a szel ényen belül igen
jelen sek: a el alajban („A” szin ) a k a c a ányának nö ekedése (59%), a „B” szin ben az agyagosodás és agyagbemosódás
kö e kez ében megnö ekede agyagás ány- a alom (45%) jellemz . A alajban zajló mállás e mékeinek ekin he goe hi , hema i ,
gipsz, alamin amo össze e k kisebb mennyiségben o dul ak el , és eloszlásuk nem mu a o e ikálisan jelen s különbségeke .
Keywo ds – c us y meadow solone z, soil mine als, saliniza ion, ex u e di e en ia ion, soil de elopmen
Tá gysza ak – ké ges é i szolonyec, alajás ányok, szikesedés, szö e i megha á ozás, alaj ejl dés
In oduc ion
In espec o hei physicochemical p ope ies,
ho izons o solone z soil p o iles a e excep ionally
di e en ia ed as a esul o hei de elopmen . This
di e en ia ion is exp essed also in hei di e en mine al
composi ion. Fo me publica ions con ain da a abou
mine al composi ion o solone z soils om di e en
loca ions (GEREI-RAKONCZAI 1985, STEFANOVITS 1999,
2003, KUTI e al. 2003), some o hem also desc ibed
mine al ans o ma ions (KUTI e al. 2003, SZÉKY-FUX –
SZEPESI 1959, SZÖ!R e al. 1991). Ou aim was o desc ibe
he mine al composi ion o a p o ile and o compa e i wi h
o he solone z soils o Hunga y.
Ma e ials and me hods
A meadow solone z soil p o ile in Püspökladány
(Pl/15; N: 47,342589º; E: 21,077442º) co e ed wi h na u al
sho g assland ege a ion (A emisio-Fes uce um pseudo inae)
and semi- ege a ed halophy ic plan communi ies
(Campho osme um annuae). The p o ile was sampled
acco ding o gene ic ho izons. Mine al composi ion o each
ho izon was de e mined by X- ay di ac ion and he mal
analysis. Gene ic ho izons we e sepa a ely sampled,
because he desc ip ion o possible soil mine alogical
p ocesses wi hin he p o ile was aimed. The e o e
composi ion o each ho izon was compa ed wi h he
composi ion o he “C” ho izon (180–200cm dep h), which
was used as e e ence, being he supposed pa en ma e ial
o soil o ming p ocesses. The las assump ion is no
comple ely ul illed, because he “C” ho izon is
pe manen ly sa u a ed wi h wa e , and he e o e modi ied
by i s sodium- ich cha ac e . Bu su ely his ma e ial is less
in luenced by soil e olu ion han he “A” and “B”
ho izons. Table 1 p esen s he basic soil da a o he
ho izons. F om mo phological poin o iew he p o ile
could be cha ac e ized by a e y shallow, g ayish elu ial
„Ahe” ho izon wi h s uc u eless, loose sandy ex u e,
which ma e ial in udes in o he s uc u al c acks o he
„B” ho izon, and shows solodiza ion cha ac e is ics
(SZENDREI 1980, 1999). Ho izon „B” is a blackish – da k
b own, sodic clay and humus accumula ion ho izon (Fig.1),
ha ing a columna s uc u e in 30–35cm dep h (B n1) and a
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a he p isma ic-blocky s uc u e below ha (B n2). F om 0
o 80cm he e a e no ca bona es, below ha ca bona es
occu also in o m o conc e ions o size up o 0.5cm. Also
o he conc e ions such as limoni e, manganese and gley
pa ches a e cha ac e is ic. Ho izon „Cgk” is ligh b ownish
yellow gleyic in usion loess, wi h up o 20% clay and 11%
ca bona e con en , pa ched wi h i on and manganese
oxides and hyd oxides. G oundwa e le el lays mos ly
deepe han 2m below he su ace. The ho izon sequence
o he p o ile could be desc ibed as Aeh-B n-B n(k)-Cg(k) wi h
applica ion o WRB diagnos ic soil ho izon de ini ions. The
‘k’ index in b acke s should mean ha he ca bona e
con en did no each he c i e ia o calcic ho izons
acco ding o WRB; despi e o o he , e y closely loca ed
p o iles, which ha e calcic cha ac e in “B” and “C”
ho izons. The p o ile could be classi ied in he Hunga ian
soil axonomy (SZABOLCS 1966) as solonchakized c us y
meadow solone z, which is also solodized, bu his
p ope y does no appea on he le el o classi ica ion.
gene ic ho izon
dep h o
samples (cm)
o g.ma . %
pH (H2O)
pH, (KCl)
CaCO3%
(de e mined
wi h Scheible -
calcime e )
KA
o al salini y %
NaHCO3%
S
(mg. eq./100g)
ESP%
Aeh 0-5 3.8 7.4 6.9 4.6 38 0.14 0.00 24.4 8.9
B n1 30-40 1.2 9.0 7.7 4.5 54 0.31 0.07 30.3 45.1
B n2 60-80 0.8 9.2 7.8 3.3 64 0.39 0.13 28.3 63.0
Cg 180-200 0.5 9.1 7.8 11.0 71 0.27 0.07 39.2 18.4
Table 1 Basic soil da a o Pl/15 p o ile, de e mined by Hunga ian soil labo a o y s anda ds
1. ábláza Magya alajlabo a ó iumi szab ányok alapján megha á ozo alap e alaj ada ok a Pl/15 szel ényben
Fo he X- ay analysis samples we e aken om he
ho izons lis ed in Table 1. The g ain-size ac ion >0.1mm
was emo ed by we sie ing. Samples we e ca e ully d ied
(a ca. 40°C), han homogenized and g ound wi h ce amic
mo a and pes le. Fo he mal analysis samples om
ho izons „A” (0–5cm), „B” (40–60cm) and „C” (180–
200cm) we e used. The g ain-size ac ion <0.002mm was
also sepa a ely analyzed, i was sepa a ed om samples
men ioned be o e by sedimen a ion echnique. Analyses
we e ca ied ou by De i a og aph-PC ins umen , samples
we e hea ed in he in e al 25 o 1000°C, hea ing a e:
10°C/min, in pla inum c ucible. Al2O3 p ehea ed a 1500°C
was used as e e ence ma e ial. De i a og ams we e
e alua ed by he so wa e o he ins umen based on
o me analyses (PAULIK & PAULIK 1981, SZÖ!R 1982,
SZÖ!R e al. 1984, 1991, SZÖ!R & BALÁZS 1988). The
amoun o KOH-soluble silica e was also de e mined in
each ho izon by Ged oiz’s me hod (BALLENEGGER 1962).
0% 20% 40% 60% 80% 100%
0-5
20-40
60-80
180-200
dep h o samples (cm)
<0,001 mm
0,001-0,002 mm
0,002-0,005 mm
0,005-0,01 mm
0,01-0,02 mm
0,02-0,05 mm
0,05-0,1 mm
>0,1 mm
Figu e 1 Pa icle size dis ibu ion in he p o ile Pl/15 de e mined
wi h sedimen a ion me hod
1. áb a Ülepí éses módsze el megha á ozo szemcsemé e eloszlási
ada ok a Pl/15 szel ényben
Resul s
In each ho izon qua z could be de e mined by X- ay
analysis as dominan soil mine al (Table 2). On he su ace
i s o al amoun is highe han below. En ichmen o qua z
in he opsoil („Aeh” ho izon) could be he esul o
en ichmen o p ima y qua z de i ed om he sand
ac ion o he soil because o ex u e di e en ia ion.
SZÉKY-FUX – SZEPESI (1959) epo ed e y simila e ical
dis ibu ion o qua z in solone z p o iles om Ho obágy.
When ine componen s we e leached ou and mo ed
downwa ds by illu ia ion, he ela i e p opo ion o qua z
inc eased in he opsoil.
Mica (musco i e) is p esen only in he „C” (14%) and
B n2 (11%) ho izons. I s amoun is he highes in he
deepes ho izon, i s ans o ma ion in o clay mine als in he
opsoil (abo e 60cm) can be supposed. A highe amoun o
clay mine als and he absence o mica in he opsoil may be
he esul o his mine al ans o ma ion. Because by X- ay
analysis di e en ia ion o mica om illi e is no always
clea , he sum o hei amoun s is gi en he ables and
diag ams (Table 2, Fig. 2, Fig. 4). The con en o plagioclases
is he lowes in „B n1” ho izon which is he si e o he mos
in ense mine al ans o ma ion in he p o ile. Highe
amoun s o plagioclase and mica in ho izon „Aeh” can be
he esul o ex u e di e en ia ion, in a simila manne as
in he case o qua z. Acco ding o X- ay analysis
amphibole occu s in e y small amoun s. Calci e is missing
om „Aeh” and om op o „B n” while accumula ion in
lowe „B n” ho izon could be es ablished wi h sligh ly
highe calci e con en as in ho izon „C”. I s e ical
dis ibu ion is a ec ed by he pH egula ing unc ion o
CO32- con en o pe cola ing ainwa e , o al amoun o
o ganic acid and CO32- p oduc ion o he oo sys em, and
he Na+- ich ising g oundwa e as well. The dep h o
ca bona e accumula ion a ies wi h seasonal a ia ion o
Szö , Gy. e al.: Mine alogical composi ion o gene ic ho izons o … MINERALOGY, GEOCHEMISTRY
11
pH and mois u e, which is e y ypical o his gene ic soil
ype (SZENDREI 1999). The mal analysis de e mined also
mic oc ys alline calci e wi h Mg2+. Ca bona e con en s o
he samples de e mined by Scheible calcime e (Table 1)
we e highe (by almos 2x) han he ca bona e con en s
de e mined by he mal and X- ay measu emen s. The
di e ence can be explained by he di e en p epa a ion o
samples o s anda d soil labo a o y (calcime ic) analysis,
and o XRD and DTA: samples o calcime e analysis
we e un ea ed (excep o homogeniza ion) bu o XRD
and DTA analyses he ac ion abo e 0.1mm was emo ed
by we sie ing. We suppose ha we sie ing washed ou a
pa o he ca bona e con en om he soil. On he o he
hand in lowe ho izons ca bona e occu s pa icula ly in he
o m o conc e ions, he g ain-size o which is o e 0.1mm
in diame e and hey we e also emo ed by sie ing.
Amo phous componen s a e p esen in 3–5%. KOH
soluble silica es de e mined by Ged oiz’s me hod a e less
han hal o he o al amo phous ma e ial de e mined by
XRD (Table 3). The es o he amo phous componen s
could be o he esiduals o mine al disin eg a ion (i on and
aluminium hyd oxides). Di e ences be ween ho izons in
amoun s o amo phous silica could be acili a ed by i s
mobili y i ee Na+ and K+ ions a e p esen cons i u ing
wa e soluble „wa e glass” (sodium and po assium
silica es) (SZABOLCS 1954). They ise upwa ds wi h
capilla y wa e and han p ecipi a e and accumula e on he
su ace (BAKER & SCRIVNER 1985).
gene ic ho izon
dep h o samples (cm)
mon mo illoni e
illi e/mon mo illoni e
illi e+musco i e
kaolini e
chlo i e
qua z
K- eldspa
plagioclase
amphibole
calci e
dolomi e
hema i e
goe hi e
gypsum
amo phous
Aeh 0–5 10 5 9 2 59 2 8 1 1 3
B n1 30–40 19 6 15 2 3 40 3 5 2 5
B n2 60–80 8 9 11 5 43 2 10 1 6 1 1 + 3
Cg 180–200 10 5 14 6 44 2 9 5 1 + 4
Table 2 Mine al composi ion (%) in gene ic ho izons o p o ile Pl/15 de e mined by he X- ay di ac ion analysis
2. ábláza Rön gendi akciós elemzéssel megha á ozo ás ányos alko ók (%) a Pl/15 szel ény gene ikus szin jeiben
gene ic
ho izon
dep h o
samples (cm)
KOH soluble
silica es (%)
amo phous
by XRD (%)
Aeh 0–5 0.95 3
B n1 30–40 1.71 5
B n2 60–80 1.03 3
Cg 180–200 0.99 4
Table 3 Amoun o KOH soluble silica es de e mined by
Ged oi z’s me hod and amo phous componen s based on X- ay
di ac ion analysis in he Pl/15 p o ile
3. ábláza A KOH-ban oldha ó sziliká ok (Ged oi z módsze e
sze in ) és az amo össze e k mennyisége ön gendi akciós
elemzés alapján a Pl/15 szel ényben
0% 10% 20% 30% 40% 50%
Aeh (0-5 cm)
B n (30-40 cm)
B n (60-80 cm)
Cgk (180-200 cm)
gene ic ho izon /
dep h o sam ples (cm)
mon mo illoni e illi e-mon mo illoni e mixed s uc u e
illi e+musco i e chlo i e
kaolini e
Figu e 2 Ve ical dis ibu ion o clay mine als in he Pl/15
p o ile based on X- ay di ac ion analysis
2. áb a Agyagás ányok e ikális eloszlása a Pl/15
szel ényben, ön gendi akciós elemzés alapján
To al amoun o clay mine als in „B n1” is mo e han
wice as much, as in he „A” ho izon (Fig. 2). In ho izon
„Aeh” he p opo ion o clay mine als de e mined by XRD
(26%) is signi ican ly highe han he p opo ion o pa icle
size ac ion <2µm (11.5%). I means ha conside able
pa o clay mine als in he „Aeh” alls in he size ac ion
>2µm. The same is he case in he uppe ho izon „B n1”
(clay mine als by XRD: 45%, ac ion <2µm: 34.1%) and in
he lowe ho izon „B n2” (clay mine als: 33%, ac ion
<2µm: 27.5%) and in ho izon „Cg” (clay mine als: 35%,
ac ion <2µm: 19.5%). In he las case, an unchanged
mine al composi ion o he o iginal sedimen can be
supposed while in he opsoil he e a e clay mine al
agg ega es o pa icle size >2µm p oduced by e y in ense
wea he ing o p ima y mine als (mos ly mica and
eldspa s). In he same ime illu ia ion o colloidal (<2µm)
dissolu ion esiduals (amo phous silica es, i on, and
aluminium hyd oxides) may explain he highe colloid
p opo ion in he „B” ho izon. Among he h ee-laye clay
mine als mon mo illoni e is dominan , i s highes amoun
is in he B n1 ho izon. The amoun o illi e/mon mo illoni e
mixed-laye clay mine als is lowe han ha o
mon mo illoni e and shows a maximum in he lowe „B n2”
ho izon. Illi e is missing in „C” and in he lowe „B n2”, bu
as men ioned be o e i s amoun is gi en oge he wi h mica
because o hei p oblema ic di e en ia ion. In he opsoil
(“A”) i s amoun is nea ha o mon mo illoni e. Chlo i e
is p esen in all ho izons bu e e ywhe e in e y small
quan i y, i s amoun inc eases wi h dep h. In he uppe
„B n1” ho izon also mino kaolini e could be de ec ed. The
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mos in ense mine al ans o ma ion p oducing clay
mine als can be supposed in he opsoil. The dis ibu ion
o clay mine als is in luenced also by illu ia ion and
accumula ion o he colloid pa icles in he „B” ho izon.
Low quan i ies o i on oxides (hema i e: Fe2O3), and oxy-
hyd oxides (goe hi e: FeO(OH)), u he mo e dolomi e
(CaMg(CO3)2) and e apo i es like gypsum (CaSO4·2H2O)
we e ound o be inal p oduc s in decomposi ion o
silica e mine als. No o he sal mine als could be de ec ed
in he samples wi hou any u he ea men , bu om sal
c us s and powde -like sal e lo escence hena di e
(Na2SO4), na on (Na2CO3·10H2O) and ona
(Na3CO3(HCO3)·2H2O) ha e been iden i ied by X- ay
analysis. VAN UFFELEN (2002) desc ibed also occu ence
o mi abili e (Na2SO4·10 H2O) close o ou sampling si e
(a a dis ance o 5–7km).
The analysis o he de i a og ams con i med, ha he
dominan s uc u e o he clay mine als is smec i e, he
subdominan s uc u es a e he mixed-laye s (p obably
illi e/mon mo illoni e). The empe a u e in e al o
dehyd oxila ion indica es a ypical s uc u es, which can be
he esul o mine al deg ada ion because o alkaliniza ion
(Fig. 3). Smec i e could be desc ibed as Na-mon mo illoni e
in he opsoil and Ca-mon mo illoni e in he pa en ock.
gene ic
ho izon
dep h o
samples
(cm)
clay
mine als
(%)
ca bona es
(%)
o ganic
ma e
(%)
Aeh 0-5 21 - 2.19
B n 40-60 34 2.88 1.43
Cg 180-200 19 2.57 0.81
Table 4 Clay mine al, ca bona e and o ganic con en s (%) in
gene ic ho izons o p o ile Pl/15 de e mined by he mal
analysis
4. ábláza A Pl/15 szel ény gene ikai szin jeinek
agyagás ány-, ka boná -, és sze esanyag- a alma a e mikus
elemzés alapján
Figu e 3 TG, DTG and DTA cu es o samples om ho izons „A”, „B” and „C” o Pl/15 p o ile.
3. áb a A Pl/15 szel ény “A”, “B” és “C” szin jeib l szá mazó min ák TG, DTG és DTA gö béi
Ve ical dis ibu ion o qua z in solone z soils
om di e en loca ions
0,1
0,2
0,3
0,4
0,5
0,6
0,7
0,8
0,9
1
0% 20% 40% 60% 80%
Püspökladány Apaj
Abádszalók Pázmánd
Szabadkígyós
Ve ical dis ibu ion o eldspa s in solone z
soils om di e en loca ions
0,1
0,2
0,3
0,4
0,5
0,6
0,7
0,8
0,9
1
0% 5% 10% 15% 20% 25%
Püspökladány Apaj
Abádszalók Pázmánd
Szabadkígyós
Ve ical dis ibu ion o mica in solone z soils
om di e en loca ions
0,1
0,2
0,3
0,4
0,5
0,6
0,7
0,8
0,9
1
0% 5% 10% 15% 20% 25%
Püspökladány Apaj
Abádszalók Pázmánd
Szabadkígyós
Ve ical dis ibu ion o clay mine als in
solone z soils om di e en loca ions
0,1
0,2
0,3
0,4
0,5
0,6
0,7
0,8
0,9
1
0% 10% 20% 30% 40% 50%
Püspökladány Apaj
Abádszalók Pázmánd
Szabadkígyós
Figu e 4 Ve ical dis ibu ion o mean mine al componen s in 4 solone z p o iles (GEREI & RAKONCZAI 1985, STEFANOVITS 1999,
STEFANOVITS 2003, KUTI e al 2003) and in he p o ile o Püspökladány (Pl/15) based on X- ay analysis. Ve ical scale in me es.
4. áb a Á lagos ás ányos össze é el e ikális eloszlása 4 szolonyec szel ényben (GEREI & RAKONCZAI 1985, STEFANOVITS 1999,
STEFANOVITS 2003, KUTI e al 2003) és a püspökladányi szel ényben (Pl/15) ön gen elemzés alapján. A ügg leges skála mé ékegysége mé e .
Discusion
As new esul s in he mine alogy o Hunga ian
solone z soils DTA analysis es ablished he p esence o
Na-mon mo illoni e in he uppe ho izons. NEMECZ (2006)
poin s ou ha i can be an in e media e p oduc o
hyd olysis, being be ween albi e and kaolini e. The Na-
cha ac e o he mon mo illoni e causes nume ous
un a ou able physicochemical p ope ies o hese soils, and
may play impo an ole in egula ion o Na con en o soil
solu ions (KUTI e al. 2003).
Szö , Gy. e al.: Mine alogical composi ion o gene ic ho izons o … MINERALOGY, GEOCHEMISTRY
13
The dis ibu ion o he amoun o KOH-soluble
silica es showed poo simila i y o e ical dis ibu ion o
he amo phous ma e ial indica ed by X- ay analysis. Thei
maximum alue could no be measu ed on he su ace –
which migh ha e been supposed by physicochemical
p ope ies o he „Aeh”ho izon – bu in he „B n” ho izon.
Also i s alue in he „C” ho izon was lowe han ha in he
„B n1” ho izon. I sugges s in ense mine al ans o ma ion
in he „B” ho izon. The e y di e en chemical and
physical p ope ies o „A” a e a he he inal esul o he
mine al ans o ma ion p ocesses ac i e in deepe le els.
Semi-quan i a i e mine al composi ions o o he
solone z soils based on X- ay analysis a e a ailable om
o me publica ions. Da a o p o iles om Apaj (KUTI e
al. 2003), Szabadkígyós (GEREI & RAKONCZAI 1985),
Pázmánd (STEFANOVITS 1999), Abádszalók (STEFANOVITS
1999, 2003), Zabszék (KUTI e al. 2003) we e compa ed
wi h ou da a om Püspökladány (Fig. 4). Also KAPOOR e
al. (1986) published esul s on solone z soils om
Ho obágy, bu hei quan i a i e da a conce n only he
sand ac ion o each ho izon, and he e o e hey a e no
compa able wi h ou da a.
In he p o iles compa ed, he mine al composi ions o
ho izon „C” a e only sligh ly di e en , howe e , mo e
signi ican di e ences could be obse ed in he
composi ion o ho izons „A” and „B”. The solone z
p o ile om Püspökladány has low eldspa and he highes
qua z con en in i s opsoil as compa ed o he o he
p o iles, while he eldspa and qua z con en s o he „C”
ho izon do no show signi ican di e ences om he
pa en ock o o he p o iles. On he o he hand, he clay
mine al con en o he „B” ho izons in Püspökladány is
seemingly e y high in compa ison wi h o he p o iles. This
is pa ly due, howe e , o he di e en de ini ion o he
micaceous mine als musco i e and illi e. When he sum
clay mine als + mica is conside ed, he di e ence be ween
he “B” ho izons o he Püspökladány and o he p o iles is
much lowe .
Al hough he e a e di e ences in mine al composi ion
o soil ho izons „A” and „B”, he mine al composi ion o
ho izon „C” o he Püspökladány p o ile does no di e
signi ican ly om he pa en ock o o he Hunga ian
solone z soils. We ha e o conclude ha a Püspökladány
in ho izon “B” he soil de eloping p ocesses p oduced
high amoun s o seconda y mine als (clay mine als)
consequen ly, lowe amoun s o p ima y mine als
( eldspa s) emained in ho izons „A” and „B”. The e y
high qua z con en o he opsoil could be he esul o
ex u e di e en ia ion: one pa o he clay pa icles
p oduced in he opsoil we e leached ou om ho izon „A”
and en iched in „B” while la ge qua z pa icles emained
hei and became ela i ely en iched nea he su ace. This
indica es long and in ense o mine al di e en ia ion
p ocesses in he solone z soils s udied.
Acknowledgemen s
We would like o exp ess ou special hanks o Tibo
Tó h (HAS RISSAC) o e iewing he i s e sion o he
manusc ip and o Is án Viczián (GIH) o his e y use ul
ema ks. The in es iga ion was suppo ed by he Ea h
Sciences PhD School, Facul y o Sciences, Uni e si y o
Deb ecen.
Re e ences
BAKER, J.C., SCRIVNER, C.L. 1985: Simula ed mo emen o
silicon in a ypic Hapludal . Soil Science, 139, 255–261
(ci . KAPOOR e al. 1986)
BALLENEGGER R. 1962: A ko asa és alumíniumhid á
megha á ozása a alaj 5%-os lúgos ki ona ában. – In:
BALLENEGGER R., DI GLÉRIA J. (ed.): Talaj- és
ágya izsgála i módsze ek. – Mez gazdasági P ess,
Budapes , 171–172
GEREI L., RAKONCZAI J. 1985: A szabadkígyósi pusz a
alajainak ön gendi akciós izsgála a. Al öldi
Tanulmányok, 9, 33–51
KAPOOR B.S., RÓZSAVÖLGYI J., RÉDLY L.-NÉ 1986: Szikes
és é i alajok izikai-kémiai ulajdonságainak és ás ányi
össze é elének izsgála a. Ag okémia és Talaj an, 35(3-4),
317–337
KUTI L., TÓTH T., KALMÁR J., KOVÁCS-PÁLFFY P. 2003:
Szikes alajok ás ányi össze é ele és ecens
ás ányképz dés Apajpusz án és Zabszék é ségében.
Ag okémia és alaj an, 52 (3-4), 275–292
NEMECZ E. 2006: Ás ányok á alakulási olyama ai
alajokban. – Academic P ess, Budapes , 324 p.
PAULIK, J., PAULIK, F. 1981: Simul aneous he moanaly ical
examina ions by means o he De i a og aph. –
Else ie
STEFANOVITS P. 2003: Szabálysze "ségek a alajás ányok
e üle i eloszlásában. – In: CSORBA P. (ed.):
Kö nyeze édelmi mozaikok. – Tisz ele kö e Ke ényi
A ila 60. szüle ésnapjá a, Deb ecen, 215–226
STEFANOVITS P. (ed.) 1999: Talajképz dési olyama ok. –
In STEFANOVITS P. (ed.): Talaj an 234–299
SZABOLCS I. 1954: Tiszán úli szikes alajaink
szologyosodása (deg adációja). Ag okémia és Talaj an,
3(4), 361–368
SZABOLCS I. (ed.) 1966: A gene ikus üzemi alaj é képezés
módsze köny e. – OMMI, Budapes , 199–205
SZÉKY-FUX V., SZEPESI K. 1959: Az „al öldi” lösz sze epe
a szikes alajképz désben. Föld ani Közlöny, 89(1), 53–
64
SZENDREI G. 1980: Szologyos é i szolonyec alajok
mik omo ológiai izsgála a. Ag okémia és Talaj an,
29(1-2), 183–198
SZENDREI G. 1999: Hazai szikes alajok mik omo ológiája.
Ag okémia és Talaj an, 48(3-4), 481–490
SZENDREI, G., TÓTH, T., SZAKÁLL, S., KOVÁCS-PÁLFFY, P.,
SAJÓ, I. 2006: Sal mine als in e lo escences on soil
su ace o Hunga y. Ac a Mine alogica-Pe og aphica,
Abs ac Se ies 5, p. 115
SZÖ!R GY., BALÁZS É., BOHÁTKA S. 1984:
Agyagás ányok, ka boná ok, szul á ok együ es
megha á ozása össze e e moanali ikai módsze ekkel.
Épí anyag, 36(9), 274–277
SZÖ!R GY., BALÁZS É. 1988: A mez ú i bu koló égla
elüle én apasz alha ó ás ányki álás ól. Épí anyag,
40(6), 217–222
SZÖ!R GY., RAKONCZAI J., DÖVÉNYI Z. 1978: A
szabadkígyósi pusz a alajainak izsgála a

ACTA GGM DEBRECINA Geology, Geomo phology, Physical Geog aphy Se ies Vol. 3 2008
14
de i a og á iás és in a ö ös spek oszkópiás
módsze el. Al öldi Tanulmányok, 2, 75–99
SZÖ!R, GY. 1982: De i a og aphic examina ions o soils
o soil mechanical and cons uc ions geological
applica ions. – IV. Cong ess In e na ional Associa ion
o Enginee ing Geology, Vol 6. Th. 3. New Delhi,
213–219
SZÖ!R, GY., SÜMEGI, P., BALÁZS, É. 1991: Sedimen ological
and geochemical analysis o uppe pleis ocene paleosols
o he Hajdúság egion, NE Hunga y. – In: PÉCSI, M.,
SCHWEITZER, F. (ed.): Qua e na y en i onmen in
Hunga y. – S udies in Geog aphy in Hunga y 26,
Academic P ess, Budapes , 47–59
VAN UFFELEN, CH. 2002: P elimina y epo on ield
campaigns o Hunga y. – Wageningen Uni e si y,
Facul y o En i onmen al Sciences, msc ., 14