Ecological-hydrological and genetic features of chernozem-like soils of closed depressions in the northern Tambov Lowland

176

ISSN 1064-2293, Eurasian Soil Science, 2008, Vol. 41, No. 2, pp. 176–189. © Pleiades Publishing, Ltd., 2008.Original Russian Text © F.R. Zaidelman, A.S. Nikiforova, L.V. Stepantsova, V.N. Krasin, S.B. Safronov, 2008, published in Pochvovedenie, 2008, No. 2, pp. 198–213.

INTRODUCTION

In 1880, Dokuchaev [4] paid attention to “smalldepressions in the dry high steppe where the light grayvegetative layer was 5–15 cm thick.” He considered thestagnation of “spring and rain water” in such depres-sions as a reason for the formation of soils with light-colored horizons. Izmail’skii, Williams, and Frantses-son [2, 9, 14] emphasized the importance of shallowsaucer-shaped depressions for the water regime of thesurrounding chernozems. The data on the meadowchernozems of depressions in the northern TambovLowland are sparse. Akhtyrtsev et al. [1] refer thesesoils to surface–gley–eluvial gray forest soils. Until thepresent time, the water regime of these soils and itseffect on the productivity of crops has not been studied.

In the last ten years, the area of waterlogged soils inthe forest-steppe zone of Russia is increasing greatly[10, 13]. According to the official data, in Tambovoblast, for the last 5 years, the area of waterlogged andbogged agricultural lands has increased by 60 thousandhectares [3]. A reason for this dangerous phenomenonis considered to be the redistribution of surface runoffand the total rise of the ground water table [11, 12].Waterlogging is characteristic for the soils of open andclosed depressions located on watershed areas and riverterraces as well. In most cases, such areas are excludedfrom crop rotation. They are grown with

Beckmannia

,canary grass, and sedges (under intense bogging). Thewaterlogging of soils causes temporary or permanent

reduction conditions and development of gley withintheir profiles [6, 7].

Earlier, we investigated the soils of open depres-sions in the northern Tambov lowland [8]. The aim ofthis work is to study the specific features of the oil gen-esis, the water regime in closed depressions, and itsinfluence on the morphology and hydrological proper-ties of the soils and productivity of crops in years dif-ferent in moisture conditions.

OBJECTS AND METHODS

Soils of two catenas were the objects of this study.The first catena was chosen on the experimental field ofthe training farm “Komsomolets” (Michurinsk district,Tambov oblast) in a closed depression (diameter100 m) on the watershed of the Ilovai and Lesnoi Vor-onezh rivers. The following soils were studied there: achernozem-like soil on the most elevated parts of thedepression, a podzolized chernozem-like soil in themiddle part of the depression slopes, and a gleyic pod-zolic chernozem-like soil in the central part of its bot-tom. The depth of the depression was about 1.5–1.7 m.The parent rock is yellow-brown fine-porous loess-likeloamy clay. Additional moistening was provided by theslope runoff of fresh water (mineralization 0.2 g/l). Theground water table was deeper than 10 m and did notaffect the water regime of all the soils. In the centralparts of the depression, the crops got wet; on its slopes,the crop yield is low. The depression was divided into

SOILPHISYCS

Ecological–Hydrological and Genetic Features of Chernozem-Like Soils of Closed Depressions

in the Northern Tambov Lowland

F. R. Zaidelman

a

, A. S. Nikiforova

a

, L. V. Stepantsova

b

, V. N. Krasin

b

, and S. B. Safronov

b

a

Faculty of Soil Science, Moscow State University, Leninskie gory, Moscow 119991, Moscow, Russia

b

Michurinsk State Agrarian University, Michurinsk, 393760 Russia

Received July 18, 2006

Abstract

—Specific features of the genesis and water regime of soils in closed depressions were studied in twocatenas located on the interfluvial and terrace surfaces. In humid years and in the years with moderate precipi-tation, the surface flooding up to early May reduced the Eh values up to 60–100 mV in the soils of the interflu-vial depressions. The contrasting stagnant–percolate water regime under the surface waterlogging caused pod-zolization of the soils manifested in the skeletans, iron nodules, humus cutans, and podzolic horizons. The pro-files acquired eluvial–illuvial differentiation, and the water–physical properties of the soils became lessfavorable. In the soils of the terrace depressions upon bogging due to the shallow ground water and stagnationof water up to mid-July, the Eh values decreased to –20 to –80 mV. The reductive conditions were responsiblefor the appearance of the morphochromatic signs of gley. The ground water of bicarbonate–calcium composi-tion at a depth of 80–120 cm hindered podzolization. The soils with features of gley and podzolization are low-productive.

DOI:

10.1134/S1064229308020099

EURASIAN SOIL SCIENCE

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ECOLOGICAL–HYDROLOGICAL AND GENETIC FEATURES 177

two parts by a road. The greater part of this depressionwas occupied by clover (variety “Vys,” sown in 2002),the other one by the rotation green fallow—winterwheat—barley—corn for silage.

The second catena was located in a large closeddepression (with a diameter of about 300 m and a depthof 1.0–1.2 m) on the first terrace above the floodplain ofthe Lesnoi Voronezh River (the territory of the trainingfarm “Roshcha,” Michurinsk district). The sequence ofthe soils studied was represented by a weakly gleyedchernozem-like soil on a flat area, a marbled gleyicchernozem-like soil on the slopes, and a gley cher-nozem-like soil in the central part of the depression.The soil-forming rocks are calcareous sandy–loamyalluvial deposits. The moistening of the soils was due tohard ground and surface water. The ground water isbicarbonate–calcium with mineralization of 1.4

−

1.8 g/l.On this area, except for the depression proper, highyields of crops were grown, but, in the last two years,this plot was abandoned because of excessive moisten-ing.

The investigations of the water regime and soil pro-ductivity were conducted in years with different mois-ture. For the winter periods (October–March), in 2003(dry year) 98% of the precipitation fell; in 2004(droughty), 74%; and, in 2005 (moist), 24%. The totalwinter precipitation was 165, 211, and 296 mm, respec-tively. In the summer, the years of 2003, 2004, and 2005were supplied with precipitation of 21, 67, and 57%;the total summer precipitation was 387, 301, and315 mm, respectively.

The field moisture of the soils was determined inthree replicates every ten days using the weightmethod. The samples were taken by an auger to a depthof 100 cm with an interval of 10 cm. The particle-sizecomposition was analyzed using the pyrophosphatemethod modified by Dolgov and Lichmanova. The den-sity of the solid phase was determined using the bottlemethod; the maximum hygroscopic moisture and min-imum (field) water capacity, using the Nikolaev methodof gypsum plates; the moisture of stable wilting, usingthe method of vegetation miniatures with the wheatvariety “Mironovskaya-808”; and the Eh, using theecotest and a platinum electrode under field conditions.The productivity of crops was assessed on plots of 1 m

2

.The density of the soils was determined in ten replicatesfor the upper horizons and in four replicates for thelower ones. Statistical processing of the data wasaccomplished according to Dospekhov.

RESULTS AND DISCUSSION

Soils of the first catena (moistened and waterloggedby surface water)

Pit 1. Thick loamy–clayey medium-humus cher-nozem-like soil on the calcareous mantle loam.

Ap, 0–30 cm. Dry, dark gray, friable, loamy–clayey,crumb–fine granular, earthworm passages and plant

roots, coprolites; the boundary is even; the transitionis distinct.A1, 30–78 cm. Fresh, moist in the lower part; darkgray, friable, loamy–clayey, fine granular; earth-worm passages and plant roots occur; coprolites;slight siliceous powdering on ped faces; the bound-ary is wavy, the transition is gradual.AB, 78–90 cm. Moist, brown, friable, loamy–clayey, crumb structure, with many dark graytongues; earthworm passages, few plant roots; slightsiliceous powdering on ped faces; the boundary istonguing, the transition is distinct.B1, 90–105 cm. Moist, yellow-brown, compact,loamy–clayey, crumb structure, earthworm passagesand plant roots; effervesces with HCl in someplaces; the boundary is even, the transition is grad-ual.B2ca, 105–150 cm. Moist, wet in the lower part;yellow-brown, compact, loamy–clayey, weak pris-matic structure, fine-porous; numerous calcareousmottles and pseudomycelium; effervesces with HCl,the boundary is even, the transition is gradual.Cca, 150–250 cm. Wet, yellow-brown, compact,loamy–clayey, prismatic; many hard (two-ply whenbroken) irregularly shaped and oval calcareous nod-ules of 3–5 cm (zhuravchiki), with calcareous coat-ings restricted to fissures; effervescence with HCl.Pit 2. Medium-thick loamy–clayey low-humus pod-

zolized chernozem-like soil on mantle loam.Ap, 0–25 cm. Moist, dark gray, light gray upon dry-ing, compact, loamy–clayey, weak crumb-granularstructure; very few fine iron nodules (1 mm andsmaller), plant roots; the boundary is even; the tran-sition is gradual.A1, 25–40 cm. Moist, dark gray, light gray upondrying, compact, loamy–clayey, weak crumb–gran-ular structure; plant roots, few fine nodules; theboundary is wavy; the transition is distinct.A1A2, 40–53 cm. Moist, gray with whitish hue,compact, loamy, weak crumb structure, nodules (upto 3 mm) and mottles of iron accumulations, plantroots; the boundary is even, the transition is distinct.A2B, 53–68 cm. Moist, light brown, whitish upondrying; compact, loamy–clayey, crumb structure,nodules, many manganic segregations (up to 1–2 cm),plant roots; the boundary is wavy, the transition isdistinct.B1, 68–90 cm. Moist, brown, compact, loamy–clayey, crumb–prismatic structure, many coatingson ped faces and manganic neoformations (3–4 mm);the boundary is even, the transition is distinct.B2, 90–140 cm. Moist, brown, compact, loamy–clayey, crumb–prismatic structure, few coatings.Pit 3. Shallow loamy low-humus podzolized cher-

nozem-like soil on mantle loam.

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ZAIDELMAN et al.

Ap, 0–10 cm. Moist, gray and light gray upon dry-ing, friable, loamy, weak crumb structure; nodulesand rusty mottles, plant roots; the boundary is even,the transition is distinct.A1, 10–30 cm. Wet, gray and whitish gray upon dry-ing, compact, loamy, weak fine granular structure;few rusty mottles, nodules; the boundary is even, thetransition is abrupt.

Ä2

fsg

/

, 30–50

cm. Wet with seeping water, dove-gray and whitish upon drying, weakly compact,loamy–clayey, crumb structure, few iron nodules;the boundary is tonguing, the transition is distinct.

Ä2Ç

g

/

, 50–70

cm. Wet with seeping water, brown-dove and whitish upon drying, compact, loamy–clayey, crumb structure, few nodules; the boundaryis tonguing, the transition is distinct.B1

g

//

, 70–100

cm. Moist, brown, very compact,loamy–clayey, prismatic structure, many coatingson ped faces, few black iron–manganic segregations(< 1 mm); the boundary is even, the transition isgradual.B2

g

//

, 100–130

cm. Moist, brown, compact, loamy–clayey, prismatic, few gray coatings on ped faces,black iron–manganic segregations (< 1 mm); theboundary is even, the transition is gradual.

ë

g

//

, 130–170

cm. Moist, brown, compact, loamy–clayey, crumb–prismatic; few iron–manganic segre-gations.

Soils of the second catena (moistened and waterlogged by atmospheric precipitation

and ground water)

Pit 4. Medium-thick loamy–clayey low-humusweakly gleyed chernozem-like soil on alluvial deposits.

Ap, 0–25 cm. Moist, dark gray, compacted, loamy–clayey, crumb–granular structure; coprolites, plantroots; black nodules (1–2 mm); the boundary iseven, the transition is gradual.A1, 25–43 cm. Moist, dark gray, slightly com-pacted, loamy–clayey, granular; coprolites, manyearthworm passages and plant roots; black roundnodules (1–2 mm); the boundary is tonguing, thetransition is distinct.

ÄÇ

g

/

, 43–51

cm. Moist, dark brown with signs ofgley and iron accumulation, weakly compacted,loamy–clayey, crumb–granular structure, few nod-ules; the boundary is wavy, the transition is distinct.

Ç

g

/

, 51–120

cm. Moist, light brown, signs of gleyand iron accumulation, compact, loamy–clayey,crumb structure, carbonized plant roots; the bound-ary is wavy, the transition is noticeable.Cca, 120 cm and deeper. Wet with seeping water,light brown, compact, clayey, structureless; impreg-nated by carbonates, many angular calcareous con-cretions (2–4 cm).

Pit 5. Medium-thick marbled loamy–clayeymedium-humus gleyic chernozem-like soil on alluvialdeposits.

A0, 0–10 cm. Moist, dark gray, friable, loamy–clayey, medium- granular; remnants of the freshwa-ter fauna, many plant roots; carbonized plant frag-ments, few nodules (1–2 mm); the boundary is even,the transition is gradual.A1, 10–38 cm. Moist, dark gray, slightly compact,loamy–clayey, coarse-granular structure; coprolites,many plant roots; remnants of freshwater fauna,nodules (1–2 mm); the boundary is wavy, the transi-tion is clear.

ÄÇ

g

//

, 38–45

cm. Moist, brownish dove, compact,loamy–clayey, crumb–granular structure, mottles ofiron accumulation and iron hard bean-shaped nod-ules (3

−

4 mm); the boundary is even, the transitionis noticeable.B1mr

g

///

, 45–75

cm. Moist, marbled, dove withmany brownish mottles, compact, loamy–clayey,crumb–prismatic, manganic mottles, humus tonguesand mottles of iron accumulation, few iron hardbean-shaped concretions; the boundary is even, thetransition is noticeable.

Ç2

g

//

, 75–90

cm. Moist, brownish dove, compact,loamy–clayey, prismatic; mottles of iron accumula-tion and few manganic punctuations; the boundary iseven, the transition is noticeable.Cca, 90 cm and deeper. Wet with seeping water,brownish whitish, compact, clayey, structureless;carbonate-impregnated, large (5–7 cm), angular cal-careous concretions.Pit 6. Shallow light clayey high-humus gley cher-

nozem-like soil on alluvial deposits.A0, 0–10 cm. Moistened, dark gray with weak signsof gley and with raw-humus, friable, clayey, coarse-granular structure; many plant roots and carbonizedplant fragments, few nodules (1–2 mm); the bound-ary is even, the transition is gradual.A1g, 10–30 cm. Moist, dark gray, friable, clayey,coarse-granular structure; many plant roots; mottlesof iron accumulation, nodules; the boundary iswavy, the transition is clear.ABg, 30–38 cm. Moist, dove-brownish, compact,clayey, granular; undecomposed plant roots, mottlesof iron accumulation, and large iron hard bean-shaped concretions (up to 5 mm) consisting of twolayers with the manganic core; the boundary istonguing, the transition is noticeable.Gfs, 38–55 cm. Moist, dove, weakly compact,clayey, crumb structure, some iron mottles, maxi-mum of bean-shaped concretions (boboviny) (3–5 mm);the boundary is tonguing, the transition is notice-able.B2, 55–65 cm. Moist to wet, brownish dove, clayey,crumb–prismatic; manganic mottles, bean-shaped


Vol. 41

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concretions; the boundary is even, the transition isgradual.Cca, 65 cm and deeper. The horizon of seepingwater, light brown clay, structureless; abundantangular calcareous concretions.The favorable water regime and insignificant addi-

tional moistening characteristic of the chernozem-likesoil of the first catena determines the formation of athick dark gray humus horizon with a fine granularstructure (Table 1, 2). The further increase in the degreeof hydromorphism leads to a reduction in the thicknessof the humus horizon, its lighter color, and degradationof the structure. Gleying under the stagnant–percolativewater regime results in the appearance of signs of pod-zolization in the soils of surface moistening. At the ini-tial stage of the excessive moistening characteristic ofthe chernozem-like soils, the following features ofhydromorphism are typical: slight siliceous powderingon ped faces throughout the soil profiles, an abundanceof skeletans in the lower part of the A1 horizon; in thepodzolized part, abundant siliceous powdering and theformation of a light-colored horizon up to 15 cm thick.Almost yearly but short-term flooding by surface watercreates conditions for gleying in the background of thestagnant–percolate water regime. As a consequence, in

the bottom of depressions, in the soils on leached rocks,a podzolic horizon is formed with a characteristic weakplaty structure and abundant nodules.

The soils of the second catena, being under the influ-ence of hard ground water, have a more shallow humushorizon, the thickness of which decreases with anincrease in the degree of hydromorphism. The bicar-bonate–calcium composition of the ground water pro-moted the development of the dark color and granularstructure of the soil. The long-term anaerobic condi-tions in the central part of the depression explain theincomplete decomposition of plant residues and theappearance of a brownish hue in the color of the soilhumus horizon. The rising capillary fringe from theground water table in the soils of the second catena pre-vented the downward migration of the surface water.This circumstance along with the high pH valuesretarded the development of podzolization. The pro-longed water stagnation is responsible for the reductionmedium and the morphochromatic signs of gleying,namely, the ‘cold’ colors of the soil horizons. Thelonger period of moisture stagnation results in moreintense colors of gley. In the transitional horizon of theweakly gleyed soil, mottles with cold color amountedto 10–20% of its area. In the gleyic soil, a gleyic mar-

Table 1.

The humus content, pH, and total acidity of the chernozem-like soils in closed depressions of the northern TambovLowland

Soil Horizon Depth, cmHumus

(Tyurin method), %

pH

KCl

Total acidity (mmol/100 g soil)

Soils of surface moistening and bogging

Chernozem-like, pit 1 Ap 0–30 6.22

±

0.23 5.03 8.8

A1 30–78 5.20

±

0.25 5.35 6.5

AB 78–90 3.05

±

0.31 5.98 3.4

Podzolized chernozem-like, pit 2 Ap 0–25 5.10

±

0.17 4.70 10.3

A1 25–40 5.23

±

0.29 4.74 10.2

AB 53–68 3.60

±

0.34 4.96 6.8

Gleyic podzolic chernozem-like, pit 3 Ap 0–10 4.63

±

0.45 5.00 11.1

A1 15–30 3.92

±

0.54 4.95 11.3

A2fsg

/

30–50 1.03

±

0.08 5.40 4.9

A2Bg

/

50–70 0.31

±

0.05 5.23 4.2

Soils of atmospheric and ground moistening and bogging

Weakly gleyed chernozem-like, pit 4 Ap 0–25 4.90

±

0.21 6.52 0.6

A1 25–43 4.95

±

0.18 6.36 0.4

ABg

/

43–51 1.95

±

0.11 6.38 0.5

Marbled gleyic chernozem-like, pit 5 A 0–10 6.0

±

0.26 6.60 0.5

A1 10–38 5.92

±

0.22 6.50 0.5

ABg 38–45 1.65

±

0.14 6.47 0.5

Gleyed chernozem-like, pit 6 Ag

/

0–10 9.12

±

0.64 6.52 0.5

A1g

//

10–30 8.94

±

0.55 6.52 1.1

ABg

///

30–38 2.88

±

0.22 6.28 0.5

180


Vol. 41

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ZAIDELMAN et al.

Tab

le 2

.

The

mor

phol

ogy

of th

e ch

erno

zem

-lik

e so

ils o

f cl

osed

dep

ress

ions

in th

e no

rthe

rn T

ambo

v L

owla

nd u

nder

con

ditio

ns o

f su

rfac

e or

gro

und-

wat

er m

oist

enin

gan

d bo

ggin

g

Indic

es

Soils

of

surf

ace

moi

sten

ing

and

bogg

ing

Soils

of

grou

nd-w

ater

moi

sten

ing

and

bogg

ing

cher

noze

m-l

ike

podz

oliz

ed

cher

noze

m-l

ike

gley

ic p

odzo

lic

cher

noze

m-l

ike

wea

kly

gley

ed

cher

noze

m-l

ike

mar

bled

gle

yic

cher

noze

m-l

ike

gley

ed

cher

noze

m-l

ike

Thi

ckne

ss o

f hu

mus

hor

izon

(A

+ A

B),

cm

; col

or90

±

9, d

ark

gray

68

±

7, d

ark

gray

30

±

5,

gray

to w

hitis

h51

±

7, d

ark

gray

45

±

5, d

ark

gray

38

±

4,

brow

nish

bla

ck

Stru

ctur

e of

hum

us h

oriz

onFi

ne g

ranu

lar

Wea

k cr

umb–

gran

u-la

rW

eak

crum

bC

rum

b–gr

anul

arM

ediu

m-g

ranu

lar

Coa

rse

gran

ular

Dep

th o

f eff

erve

scen

ce w

ith H

Cl,

cm10

5N

o ef

ferv

esce

nce

No

effe

rves

cenc

e12

090

65

Har

d co

ncre

tions

CaC

O

3

Tw

o-pl

y zh

urav

chi-

ki (

3–5

cm)

from

a

dept

h of

150

cm

No

No

Ang

ular

con

cret

ions

(3

–5 c

m)

from

120

cm

Lar

ge a

ngul

ar c

on-

cret

ions

(5–

7 cm

) fr

om 9

0 cm

Ang

ular

con

cret

ions

(3

–5 c

m)

from

80

cm

Fe-M

nN

oFi

ne (

1–2

mm

) br

owni

sh b

lack

nod

-ul

es in

hum

us a

nd

tran

sitio

nal h

oriz

ons

Bro

wn

nodu

les

(to

5 m

m)

in h

umus

an

d po

dzol

ic h

ori-

zons

(10

% o

f th

e m

ass)

Bla

ck n

odul

es

(1–2

mm

) in

hum

us

hori

zon

Bro

wn

bean

-lik

e (b

obov

iny)

con

cre-

tions

(to

5 m

m) i

n th

e A

Bg

hori

zon

Bro

wn

bobo

viny

(to

5

mm

) in

AB

g

Oth

er n

eofo

rmat

ions

Cal

care

ous

“mou

ld”

and

smal

l cor

ksM

anga

nic

mot

tles

in

tran

sitio

nal h

oriz

on

and

hum

us–i

ron

cu-

tans

in th

e B

hor

izon

Hum

us–i

ron

coat

-in

gs in

BM

ottle

s of

iron

acc

u-m

ulat

ion

in tr

ansi

-tio

nal h

oriz

on a

nd

carb

onat

e im

preg

na-

tion

in p

aren

t roc

k

Mot

tles

of ir

on a

ccu-

mul

atio

n in

hum

us

hori

zon

and

carb

on-

ate

impr

egna

tion

in

pare

nt r

ock

Mot

tles

of ir

on a

ccu-

mul

atio

n th

roug

hout

th

e pr

ofile

and

car

-bo

nate

impr

egna

tion

in p

aren

t roc

k

A2

hori

zon

and

sign

s of

pod

-zo

lizat

ion

Wea

k si

liceo

us p

ow-

deri

ng in

the

low

er

part

of

the

A1

hori

-zo

n

Abu

ndan

t sili

ceou

s po

wde

ring

(15

−

20 c

m

wid

e) u

nder

the

hu-

mus

hor

izon

Whi

tish

colo

r of

the

who

le p

rofi

le, A

2 ho

-ri

zon

of 2

0 cm

thic

k

No

No

No

Mor

phoc

hrom

atic

fea

ture

s of

gl

eyin

gN

oN

oG

rayi

sh d

ove

mot

tles

(20–

30%

) in

B1

Dov

e m

ottle

s (2

0%)

in A

Bg

Mar

bled

col

or o

f B

mr

Fron

tal g

leyi

ng o

f th

e up

per

part

of

the

prof

ile, G

fs h

oriz

on


Vol. 41

No. 2

2008


bled horizon was formed, 50% of its colors being coldones; in the gleyed soil, the whole part of the soil profile(up to the calcareous horizon) was gleyed.

The characteristic neoformations of the nonpod-zolized chernozem-like soils were carbonate concre-tions and thin coatings, mottles, and pseudomycelium(Table 2). The soils of the surface moistening (with thehigher degree of hydromorphism) were carbonate-free.They have neoformations related to the gley process,such as nodules in the upper soil horizons, the numberand size of which increased with increasing hydromor-phism. Their maximal amount was in the podzolizedand podzolic horizons. Another kind of neoformationswere the humus coatings in the lower part of the profilesand mangans in the transitional horizon. In the A2Bhorizon of the podzolized soil, the size of such manganswas up to 2–3 cm in diameter and that of manganicpunctuations in the B1 horizon, 2–4 mm. In the transi-tional horizon of the podzolic soil, manganic neoforma-tions were less abundant; in the B2 horizon, mottles ofdove color appeared.

In the soils of the second catena, unlike the soils ofthe first catena, both carbonate and iron neoformationswere present. The presence of the former was deter-mined by the bicarbonate composition of the groundwater. The parent rock of the soils of the second catenawas impregnated with carbonates and contained hardcalcareous concretions of irregular angular shape. Theirsizes little depended on the degree of hydromorphismof the soils, and the upper boundary of their appearanceoften coincided with the ground water table. Iron neo-formations were more diverse. They occurred in theupper part of all the soil profiles up to the boundarywith the calcareous horizon. In the weakly gleyed soil,the short-term moisture stagnation leads to the forma-tion of fine black nodules. In the gleyic and gleyedsoils, upon the longer flooding, they were larger and ofrusty brown color.

Soil physical properties: Elements of the hydrological and redox regimes; productivity of agricultural crops

The even distribution of clay and the predominanceof the coarse silt fraction were characteristic of the non-podzolized chernozem-like soil (Table 3). The contrast-ing stagnant–percolate water regime of the podzolizedsoil leads to the differentiation of the soil profileaccording to the particle-size composition. This factwas most distinctly manifested in the profile of the pod-zolized chernozem-like soil. Under conditions of thestagnant–percolate water regime, in these soils, theenvironment for active formation of concretions (10%of the soil mass) proved to be most favorable (Table 2).

The profiles of the chernozem-like soils wereformed differently under conditions of moistening withbicarbonate–calcium ground water. The shallowground water in the soils of the second catena preventedthe removal of the surface water. Therefore, the differ-

entiation of the profiles of these soils according to theparticle-size composition was weakly displayed in thesoils at the initial stage of gleying and was completelyabsent in the gleyed soils. The maximum content of theclay fraction was recorded in the gley horizons.

The two groups of the chernozem-like soils consid-ered also differed in their physical properties. The non-podzolized soil of the first catena was characterized bythe density and hydrological constants that were opti-mal for the growth and development of plants. Theporosity throughout the profile was not lower than 50%.The structure of the podzolized and podzolic soils wasdestroyed; hence, their density became higher and theporosity sharply decreased. The minimum and totalwater capacity little differed. The decrease in the num-ber of aeration pores was unfavorable for the plants. Inthis case, the lower horizons functioned as a waterproofbarrier.

The soils of the second catena have other particularfeatures. The preservation of the granular structuredetermined the optimal density and porosity of all thesoils in this catena (Table 4). The considerable contentof semidecomposed plant residues explained the highvalues of the hydrological constants in the gleyed soil.

The minimum precipitation for the cold period pre-ceding the year 2003 determined the absence ofperched water in the soil profiles of the first catena(Fig. 1). This has caused a fast increase in the redoxpotential values in the upper soil horizons (Fig. 2). Thelow expenses of clover for transpiration in the first yearof its cultivation and the high summer precipitationwere responsible for the values of the moisture in theupper horizons being close to the field capacity and notdescending below the capillary break moisture duringthe whole growing period (Fig. 1). However, the lowerhorizons of the podzolized and podzolic gleyic soilswere characterized by higher moisture as compared tothat in the nonpodzolized chernozem-like soil. Theoptimal water regime and the absence of perched waterdetermined the high yield of cereals, especially of sum-mer cereals on the nonpodzolized soil (Table 5). Theunfavorable physical properties of the hydromorphicsoils were adversely reflected in the productivity of bar-ley and winter wheat. However, the additional moisturereserves in the lower horizons of the podzolized soilsprovided a higher yield of clover (not demanding on thesoil conditions) as compared to its yield on the nonpod-zolized soil.

In 2003, the second catena was occupied by winterwheat. In this year, most of the thawed water flowed todepressions over the surface of the compact plowedsoil. Even in early May, in the weakly gleyed soil, theredox potential became favorable for the developmentof plants. Abundant rains and their even distribution inthe spring and early summer provided the moisture val-ues in the topsoil within the following range: the fieldcapacity and moisture of capillary break during thewhole growing period (Fig. 3). This circumstance

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ZAIDELMAN et al.

Table 3.

The particle-size composition of the chernozem-like soils in closed depressions of the northern Tambov Lowland(pyrophosphate method)

Soil Horizon Depth, cmContent of fractions, %; fraction size, mm

1–0.25 0.25–0.05 0.05–0.01 0.01–0.005 0.005–0.001 <0.001 <0.01

Soils of surface moistening and bogging

Chernozem-like, pit 1

Ap 0–30 3 10 28 19 21 19 59

A1 30–78 1 11 34 20 15 19 55

AB 78–90 6 6 34 21 15 18 54

B1 90–105 3 14 27 11 21 24 56

B2ca 105–150 3 11 31 22 4 19 55

Cca 150–200 9 13 25 19 10 24 53

Podzolized cher-nozem-like, pit 2

Ap 0–25 2 2 35 19 17 25 61

A1 25–40 2 1 42 15 16 24 56

A1A2 40–53 2 1 34 12 16 35 63

A2B 53–68 2 2 21 13 14 48 75

B1 68–90 2 2 25 13 11 47 71

B2 90–140 2 2 25 10 10 51 71

Gleyic podzolic chernozem-like, pit 3

Ap 0–10 3 12 37 19 17 12 48

A1 15–30 3 18 41 17 14 7 38

A2 fsg

/

30–50 12* 8 44 14 15 7 36

A2Bg

/

50–70 2 8 37 13 13 27 53

B1g

/

70–100 2 10 28 11 13 36 60

B2g

//

100–130 2 10 29 11 13 35 59

Cg

//

130–170 4 11 27 10 8 39 58

Cutans

2 10 28 7 10 43 60

Soils of atmospheric and ground-water moistening and bogging

Weakly gleyed chernozem-like, pit 4

Ap 0–25 2 5 30 14 20 29 63

A1 25–43 2 6 37 14 17 24 55

ABg 43–51 3 3 27 11 18 37 66

B2g

/

51–120 3 2 34 10 11 40 61

Cca 120–160 4 2 32 15 21 26 62

Marbled gleyic chernozem-like, pit 5

AO 0–10 2 8 42 13 14 21 48

A 10–38 12 12 37 8 11 20 39

ABg 38–45 3 3 25 12 19 39 69

B1mrg

///

45–75 6 6 25 13 10 41 63

Cca

90–150 5 7 30 11 11 36 58

Gleyed cher-nozem-like, pit 6

Ag

/

0–10 2 9 43 15 13 18 74

A1g

//

10–30 2 15 38 15 12 18 68

ABg

/// 30–38 3 2 37 11 16 31 84

Gfs 38–55 2 3 27 12 18 38 83

Cca 65–120 3 2 24 20 13 38 75

* The high content of this fraction is related to the presence of nodules.

EURASIAN SOIL SCIENCE Vol. 41 No. 2 2008

ECOLOGICAL–HYDROLOGICAL AND GENETIC FEATURES 183 Table 4. The physical properties of the chernozem-like soils in closed depressions of the northern Tambov Lowland

Soil Horizon Depth, cm

Density of soil

Density of solid phase

Porosity MH WM FWC Pa

g/cm3 % of volume

Soils of surface moistening and bogging. Catena 1

Chernozem-like, pit 1

Ap 0–30 1.04 ± 0.04 2.43 57.2 9.6 15.8 30.9 26.3

A1 30–78 1.03 ± 0.08 2.58 60.1 9.6 15.1 29.5 30.6

AB 78–90 1.20 ± 0.05 2.61 54.0 10.7 16.8 33.4 20.6

B1 90–105 1.21 ± 0.06 2.63 54.0 10.1 17.1 32.5 21.5

B2ca 105–150 1.28 ± 0.08 2.63 51.3 11.3 17.3 31.5 20.3

Cca 150–200 1.30 ± 0.04 2.63 50.6 11.5 16.8 29.3 21.3

Podzolized chernozem-like, pit 2

Ap 0–25 1.33 ± 0.07 2.46 45.9 12.8 16.6 37.6 8.3

A1 25–40 1.38 ± 0.07 2.52 45.2 13.9 15.2 33.2 12.0

A1A2 40–53 1.55 ± 0.03 2.51 38.2 14.7 15.5 32.6 5.6

A2B 53–68 1.52 ± 0.04 2.60 41.5 15.8 17.0 29.9 11.6

B1 68–90 1.62 ± 0.15 2.67 39.3 16.6 18.3 35.8 3.5

B2 90–140 1.60 ± 0.04 2.52 36.5 16.5 18.4 32.6 3.9

Gleyic podzolic chernozem-like, pit 3

Ap 0–10 1.17 ± 0.05 2.46 52.4 4.8 10.8 35.4 17.0

A1 10–30 1.48 ± 0.05 2.58 42.6 5.2 14.6 34.0 8.6

A2 fsg/ 30–50 1.51 ± 0.06 2.57 41.2 5.1 7.0 25.6 15.6

A2Bg/ 50–70 1.64 ± 0.03 2.63 37.6 4.9 7.4 28.0 9.6

B1g// 70–100 1.59 ± 0.04 2.73 41.8 9.2 14.2 28.0 13.8

B2g// 100–130 1.62 ± 0.03 2.69 39.8 9.2 17.0 28.0 11.8

C g// 130–170 1.66 ± 0.04 2.63 36.9 7.8 15.3 30.8 6.1

Soils of atmospheric and ground moistening and bogging. Catena 2

Weakly gleyed chernozem-like, pit 4

Ap 0–25 0.99 ± 0.04 2.41 58.9 11.7 12.9 35.0 23.9

A1 25–43 1.06 ± 0.05 2.49 57.4 12.0 15.4 35.4 22.0

ABg/ 43–51 1.22 ± 0.03 2.53 51.8 13.3 14.7 31.7 20.1

Bg 51–120 1.42 ± 0.10 2.62 45.8 10.7 16.8 27.4 18.4

Cca 120–160 1.42 ± 0.08 2.59 45.2 10.8 17.0 28.5 16.7

Marbled gleyic chernozem-like, pit 5

A 0–10 0.88 ± 0.05 2.42 63.6 12.5 14.0 41.8 21.8

A1 10–38 0.89 ± 0.08 2.41 63.1 11.7 12.4 41.7 21.4

ABg 38–45 1.21 ± 0.07 2.55 52.5 14.0 15.8 35.3 17.2

B1mrg/// 45–75 1.27 ± 0.12 2.66 52.2 11.2 14.4 27.1 25.1

Cca 90–150 1.44 ± 0.09 2.65 45.7 12.3 13.9 28.1 17.6

Gleyed cher-nozem-like, pit 6

Ag/ 0–10 0.71 ± 0.06 2.30 69.1 12.6 18.7 49.0 20.1

A1g// 10–30 0.79 ± 0.10 2.32 65.9 12.3 16.6 48.0 17.9

ABg/// 30–38 1.13 ± 0.05 2.45 53.9 13.5 18.0 42.1 11.8

Gfs 38–55 1.17 ± 0.03 2.53 53.8 13.7 16.9 38.0 15.8

Cca 65–120 1.31 ± 0.04 2.58 49.2 13.3 14.4 33.3 15.9

Note: MH is the maximum hygroscopic moisture, WM is the wilting moisture, FWC is the field capacity, and Pa is the air capacity.

184


ZAIDELMAN et al.

explained the high yield of winter wheat (Table 6). Thesurface flooding of the gleyed soil and moisture stagna-tion at a depth of 20 cm in the gleyic soil lasted up tolate May. These conditions changed sharply in the fol-lowing way. In the central part of the depression, thesoil was dried out down to a depth of 70 cm and, in themiddle part of its slopes, to a depth of 40 cm. This phe-nomenon was related to the active growth of perennialgrasses in the central part of the depression when themean daily temperature reached 10°ë and the reductiveconditions were replaced for the oxidative ones. Rainsfalling late in June partly compensated for the waterdeficit in the upper soil horizons and created favorableconditions for the growth and development of perennialgrasses.

The higher winter precipitation in 2004 than in theprevious years resulted in the formation of perchedwater in the podzolized and gleyic podzolic soils of thefirst catena. It remained in the upper 1-m layers up to

mid-May in the former soil and until the beginning ofthe summer in the latter soil. During the growingperiod, the main amount of precipitation was restrictedto May–June. Therefore, the moisture within the wholeprofile of the nonpodzolized chernozem-like soil wasoptimal and provided high yields of cereals. The exces-sive moistening of the podzolized and gleyic podzolicsoils became a reason for the lower values of the redoxpotential as compared to that in the nonpodzolized soil,where the yield of cereals, especially of barley, waslower. At the same time, the high moisture reserves inthe waterlogged soils contributed to the high yield ofclover.

In the autumn of 2003, the soils of the second catenawere tilled. In the spring of 2004, thawed water fullysoaked the loosened soil. The shallow ground watertable hindered the outflow of water, and, up to thebeginning of the summer, reductive conditions werepreserved even in the weakly gleyed soil. The whole

Fig. 1. The moisture regime of the soils of surface moistening and bogging: 1—chernozem-like; 2—podzolized chernozem-like;3—gleyic podzolized chernozem-like. Designations and in Fig. 3: 1—hygroscopic moisture; 2—field capacity–total water capacity;3—field capacity–moisture of capillary break; 4—moisture of capillary break–wilting moisture.



plot was covered with water pools of different sizes,and it was not used for crops. Nevertheless, in theautumn, the soil was tilled again. The water stagnatedin the surface layers of the gleyic soil up to early Mayand, in the gley soil, to mid-June. Hence, there was asharp decrease in the redox potential, and the activegrowth of perennial grasses was retarded. These events,along with the absence of rains in the second half of thesummer, adversely affected the development of plants,and their yield went down.

The year of 2005 was the moistest (among the yearsinvestigated) due to the high precipitation in the preced-ing cold period. Therefore, perched water was formedeven in the profile of the nonpodzolized chernozem-like soil of the first catena. Abundant rains in the latespring and early June prevented drying of the soils. Theperched water in the podzolized and podzolic cher-nozem-like soils was preserved in the upper 0.5-m layerup to mid-June and up to late August, respectively.Despite the fact that, in the upper layers, the soil mois-ture was higher than the total field capacity, oxygen-sat-urated rains determined the high values of the redoxpotential in the nonpodzolized and podzolized cher-nozem-like soils. The reductive conditions were pre-served only in the soil of the bottom of the depression(Fig. 2). The second half of the growing period wasdroughty and the mean daily temperatures were high.The moisture of the nonpodzolized chernozem-like soilwas lowered below the moisture of the capillary break,and the clover yield decreased. The yield of perennialgrasses on the hydromorphic soils of the first catenawhere they did not dry out was much higher.

The treatment of the soils without taking intoaccount their hydrological features has caused long-term moisture stagnation in the surface soil layers in thesecond catena (Fig. 3). Almost up to early June, theagricultural machines could not work. The untimelysowing of a vetch–oat mixture (in the second half of thesummer) was performed in the period with high tem-peratures and without precipitation. The weakly gleyedchernozem-like soil was dried out to a depth of 50 cm.The combination of unfavorable conditions resulted inthe very low yield of annual grasses. The drastic transi-tion from flooding to drying out of the gleyed andgleyic soils became a reason for the lower yield ofperennial grasses as compared to that in the previousyears.

Thus, the water regime of the soils with the surfacemoistening in the closed depressions was determinedexclusively by the winter precipitation. In the nonpod-zolized chernozem-like soil, perched water wasobserved during short periods and only in the yearswith high winter precipitation. The soil fast becamephysically mature and suitable for planting of regionalvarieties of crops. In the years moderately suppliedwith winter precipitation, perched water existed in the1-m layer of the podzolized soil up to mid-May; in themoist years, it remained there up to late June. In dry

years and in years with moderate precipitation, wintercereals may be cultivated there; summer cereals oftenperish. The additional moisture reserves provide a sta-ble yield of perennial legumes and grasses. Surfaceflooding is characteristic of the gleyic chernozem-likepodzolic soil. In the years with medium precipitation, itwas observed for 2–3 weeks and, in the years with highprecipitation, for about 1.5 months. The perched waterwas preserved in the profile of this soil up to the middleof the summer and caused the death of all the cereals.Nonetheless, even in the years weakly supplied withwinter precipitation, unfavorable physical conditionsdue to gleying do not allow normal development ofplants. Perennial grasses produced a low but stableyield.

The amount of annual precipitation affected thewater regime of the soils moistened owing to theground and surface water to a lesser extent than thesoils of the first catena. The late fall plowing is not rec-ommended for the weakly gleyed soil with a shallowground water table and small thickness of the humuslayer, since it retarded the runoff of excessive water.Soil tillage for winter cereals is acceptable only in sum-mer periods. Under such conditions, it is possible toyield a high harvest of winter cereals. The gleyic andgleyed soils are exposed to permanent excessive moist-ening and flooding irrelative of the moisture conditions

Fig. 2. The dynamics of the Eh in the soils of surface moist-ening and bogging (0–20 cm). Soils: 1—chernozem-like;2—podzolized chernozem-like; 3—gleyic podzolized cher-nozem-like.

186


ZAIDELMAN et al.

of particular years; therefore, the cultivation of thesesoils is hardly reasonable. However, perennial grassesproduce a stable yield. The areas with these soils maybe used as hayfields.

The data obtained permit one to pay attention to thefact that the podzolized and podzolic horizons areformed only in the profiles of the leached (carbonatesare deeper than 150–170 cm) soils with surface moist-ening and bogging with fresh water under conditions ofthe stagnant–percolative water regime. In the soilsmoistened or bogged with bicarbonate–calcium water(carbonates at a depth of 60–120 cm), the features of

podzolization are absent irrespective of the degree ofgleying.

CONCLUSIONS

(1) In the northern part of the Tambov Lowland, twotypes of closed depressions different in the hydrologi-cal regime and properties of the soils may be distin-guished. Some depressions are exclusively of surfacemoistening and occur on the watershed areas. The oth-ers are located on the fluvial terraces, and their waterregime is determined by the ground water (Table 7).

Table 5. The yield (t/ha) of crops on the chernozem-like soils of surface moistening and bogging in closed depressions ofthe northern Tambov Lowland in differently moist years

Year Crop

Soil

hernozem-like podzolized chernozem-like

gleyic podzolic chernozem-like

2003 Wheat1 35.5 ± 4.3 26.2 ± 1.4 12.2 ± 0.7

Barley2 55.2 ± 7.2 42.9 ± 3.2 –

Clover3 72 ± 13 215 ± 12 295 ± 15

2004 Wheat1 48.7 ± 5.6 32.6 ± 4.7 0

Barley2 23.6 ± 2.5 12.3 ± 0.8 *

Clover3 210 ± 8 310 ± 11 280 ± 9

2005 Wheat1 46.0 ± 4.4 31.5 ± 1.6 0

Barley2 17.5 ± 3.8 1.9 ± 0.5 *

Clover3 165 ± 10 320 ± 12 264 ± 9

Note: Here and in Table 6, dashes indicate the absence of crops on the soil in the year investigated; * indicates the absence of crops becauseof excessive moistening; 0 is the wetting. Crops: 1—winter wheat “Mironovskaya-808”; 2—spring barley “Auksinyai-3”; 3—clover“Vys”; 4—natural perennial grasses (Beckmannia, Bromopsis, timothy, and foxtail); 5—vetch “L’govskaya,” oat “Gorizont.”

Table 6. The yield (t/ha) of crops on the chernozem-like soils of surface atmospheric and ground-water moistening in closeddepressions of the northern Tambov Lowland

Year Crop

Soil

weakly gleyed chernozem-like

marbled gleyic chernozem-like gleyed chernozem-like

2003 Wheat1 42 8 *

Barley4 – 219 250

2004 Clover2 * * *

Barley4 – 198 273

2005 Vetch + oats5 45 * *

Barley4 – 185 95



(2) The water regime of the depressions located onthe interfluves is determined by the precipitation of thepreceding cold period. In the years qualified as dry interms of the winter precipitation, perched water may beabsent in all the soils; in moist years, it may be pre-served in the profiles of podzolized and gleyic soils upto the mid-summer. The alternation of short-termreduction and longer oxidation periods was characteris-tic of the redox regime of the upper soil horizons.

(3) In the closed depressions of the interfluves,under the stagnant–percolative water regime, a com-plex of soils with well-pronounced features of pod-zolization (skeletans, podzolized and podzolic hori-zons) is formed. The soils are leached of carbonates; intheir upper horizons, nodules and manganic neoforma-tions are formed; in the lower part of the profiles,humus coatings were found.

(4) In the soils of surface moistening, with increas-ing hydromorphism the eluvial–illuvial differentiationof the profiles becomes stronger. In this case, the soil

structure is destroyed and the lower horizons becomemore compact.

(5) Stable crops of cereals are difficult to be yieldedon the soils of surface moistening even in the absenceof perched water. At the same time, the productivity ofperennial grasses is high irrespective of the moisture ofthe year.

(6) The moisture of different years affected thewater regime of the soils influenced by the groundwater to a lesser degree than the soils of the surfacemoistening. In early spring, in the humus horizon of theweakly gleyed chernozem-like soil, the reductive con-ditions are quickly replaced by the oxidative ones. Adeep and long-term anaerobiosis is typical for thehighly hydromorphic soils.

(7) The permanently high level of the ground watertable and the bicarbonate composition prevents thedevelopment of podzolization features in the soils ofground-water moistening, and the long-term moisturestagnation promotes the appearance of a cold colorcharacteristic of the gley horizons. In the soil profiles,

Fig. 3. The moisture regime of the soils of ground-water moistening and bogging (0−20 cm): 4—weakly gleyed; 5—marbled gleyicchernozem-like; 6—gleyed chernozem-like.

188


ZAIDELMAN et al.

Tab

le 7

. T

he e

colo

gic-

hydr

olog

ical

cha

ract

eriz

atio

n an

d di

agno

stic

fea

ture

s of

che

rnoz

em-l

ike

soils

of

clos

ed d

epre

ssio

ns in

the

nort

hern

Tam

bov

Low

land

Soi

lW

ater

reg

ime

in m

oist

yea

r M

orph

olog

ical

sig

ns

of g

leyi

ngC

arbo

nate

ne

ofor

mat

ions

Fe–

Mn

neo

form

atio

ns C

rop

yiel

dA

gric

ultu

ral u

se

Soil

s of

surf

ace

mois

tenin

g

Che

rnoz

em-l

ike,

pit

1Pe

rcol

ativ

e, m

oist

ure

stag

natio

n fo

r 1–2

wee

ks

in m

oist

yea

rs

Slig

ht s

ilice

ous

pow

-de

ring

in A

1C

arbo

nate

coa

ting,

zh

urav

chik

i fro

m a

de

pth

of 1

50 c

m

No

Incr

ease

in c

erea

ls c

rop

by 1

0–20

% is

pos

sibl

e in

dro

ught

y ye

ars

Cul

tivat

ion

of a

ll th

e cr

ops

is p

ossi

bl

Podz

oliz

ed c

her-

noze

m-l

ike,

pit

2St

agna

tion

of p

erch

ed

wat

er f

or 1

–2 w

eeks

to 2

m

onth

s in

moi

st y

ears

Abu

ndan

t sili

ceou

s po

wde

ring

in A

1, th

e pr

esen

ce o

f th

e A

1A2

and

A2B

hor

izon

s

No

Fin

e no

dule

s in

A1

and

iron

–hum

us c

oat-

ings

in tr

ansi

tiona

l ho

rizo

ns

Dec

reas

e in

yie

ld o

f ce

-re

als

by 2

0–50

%; g

rass

yi

eld

is h

ighe

r by

40

−80%

than

that

on

leac

hed

cher

noze

m

Hay

fiel

ds a

nd p

astu

res

with

val

uabl

e le

gum

es

Gle

yic

podz

olic

che

r-no

zem

-lik

e, p

it 3

Sta

gnat

ion

of p

erch

ed

wat

er f

or a

mon

th in

Ap,

fo

r 3

mon

ths

in s

ubpl

ow

hori

zons

A2

hori

zon

of 2

0 cm

th

ick,

mot

tles

of g

ley

in th

e tr

ansi

tiona

l hor

i-zo

n

No

Nod

ules

in h

umus

ho-

rizo

n an

d ir

on–h

umus

co

atin

gs in

tran

sitio

n-al

hor

izon

Reg

ula

r over

wet

ting o

f ce

real

s: the

yie

ld o

f pe-

rennia

l her

bs

is 3

0−4

0%

hig

her

than

that

on the

leac

hed

cher

noze

m

Hay

fiel

ds

Soil

s of

surf

ace

and g

round m

ois

tenin

g

Wea

kly

gley

ed c

her-

noze

m-l

ike,

pit

4St

agna

tion

of p

erch

ed

wat

er f

or 1

–2 w

eeks

Sm

all m

ottle

s of

gle

y in

AB

g F

ine

angu

lar

nodu

les

in C

ca F

ine

nodu

les

in h

u-m

us h

oriz

onIn

med

ium

-moi

st y

ears

, hi

gh y

ield

of

win

ter

crop

s; s

prin

g cr

ops

are

unsu

cces

sful

Lat

e fa

ll pl

owin

g is

ex-

clud

ed, c

ultiv

atio

n of

sp

ring

cro

ps a

nd p

e-re

nnia

l gra

sses

is p

os-

sibl

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both calcareous and iron pedofeatures are present. Theshape and size of angular calcareous concretions andtheir distribution are determined by the compositionand level of the ground water. The size of nodulesbecomes larger with increasing degree of hydromor-phism.

(8) The soils of ground-water moistening and bog-ging are distinguished by their granular structure andoptimal density. The eluvial–illuvial differentiation oftheir profiles is weak or absent in these soils.

(9) High yields of winter cereals are possible on theweakly gleyed chernozem-like soil. However, the latefall plowing that favors excessive moistening of the soilis not recommended. Under conditions of the natural

water regime, the areas with gleyed and gleyic cher-nozem-like soils may be used as hayfields.

REFERENCES1. A. B. Akhtyrtsev, P. G. Aderikhin, and B. P. Akhtyrtsev,

Meadow-Chernozemic Soils of the Central RussianPlain (Voronezh. Gos. Univ., Voronezh, 1981) [in Rus-sian].

2. V. R. Williams, “Morphological Features of Cher-nozems,” in Works (1950), Vol. 5, pp. 547–566.

3. Report on the State of the Natural Environment and theUse of Natural Resources in Tambov Oblast (Tambov,2001) [in Russian].

4. V. V. Dokuchaev, Russian Chernozem: Selected Works(Sel’khozgiz, Moscow, 1948), Vol. 1, pp. 21–476 [inRussian].

5. F. R. Zaidel’man, Natural and Anthropogenic Waterlog-ging of Soils (Gidrometeoizdat, St. Petersburg, 1992).

6. F. R. Zaidel’man, Podzolization and Gleyization(Nauka, Moscow, 1974) [in Russian].

7. F. R. Zaidel’man, Gleyzation and Its Role in Pedogene-sis (Mosk. Gos. Univ., Moscow, 1998) [in Russian].

8. F. R. Zaidel’man, A. S. Nikiforova, and L. V. Stepants-ova, “Ecological-Hydrological Features of LeachedChernozems and Meadow-Chernozemic Soils in theNorthern Part of the Tambov Plain,” Pochvovedenie,No. 9, 1102–1114 (2002) [Eur. Soil Sci. 35 (9), 978–989(2002)].

9. A. A. Izmail’skii, Selected Works (Sel’khozgiz, Moscow,1949) [in Russian].

10. T. S. Lukovskaya, “Secondary Anthropogenic Hydro-morphism of Chernozems,” in Proceedings of the Inter-national Conference “Problems of Anthropogenic Pedo-genesis” (Moscow, 1979), Vol. 1, pp. 112–115 [in Rus-sian].

11. S. V. Ovechkin and V. A. Isaev, “Periodically Water-logged Soils of the Central Chernozemic Zone,” in Gen-esis, Anthropogenic Evolution, and Rational Use ofSoils: Proceedings of the Dokuchaev Soil Science Insti-tute (Moscow, 1989), Vol. 47, pp. 8–25 [in Russian].

12. Yu. P. Parakshin, E. M. Parakshina, and S. A. Uvarov,“Progressive Land Waterlogging in the Central Cher-nozemic Zone,” in Proceedings of the International Con-ference “Problems of Anthropogenic Pedogenesis”(Moscow, 1997), Vol. 2, pp. 22–24 [in Russian].

13. E. M. Samoilova, Meadow Soils of the Forest-Steppe(Mosk. Gos. Univ., Moscow, 1985) [in Russian].

14. V. A. Frantsesson, Chernozemic Soils: Selected Works(Sel’khozgiz, Moscow, 1963) [in Russian].

Fig. 4. The dynamics of Eh in the soils of ground-watermoistening and bogging (0−20 cm). Soils: 4—weaklygleyed; 5—marbled gleyic chernozem-like; 6—gleyedchernozem-like.

Documents

Ecological-hydrological and genetic features of chernozem-like soils of closed depressions in the northern Tambov Lowland