ROCZNIKI G LE B O ZN A W C ZE T. X X V , DODATEK, W A R S Z A W A 1974
A L O J Z Y K O W A L K O W S K I, J A N B O R Z Y S Z K O W S K I
R E SE A R C H O N T H E R EVE R SE C O U P L IN G S B E T W E E N M E SO R E LIE F A N D SO M E PR O PE R T IE S OF TH E F H H O R IZ O N IN A R U S T Y P O D Z O L IC SO IL Departm ent of soil Science and Fertilization Forest Research Institute
Experim ent Centre Sękocin
IN T R O D U C T IO N
The whole history of soils is reflected in their sequences on both the smallest and the large land areas. According to F i n к [3] their regularities can virtually be recognized only when a large-scale mapping is applied considering the features of the landscape and the Quaternary geology. A c cording to K o p p [5] the catenas and soil-associations of a definite genesis which corelate with biotopic chains of plant associations are shown in the legend of the large-scale soil maps. They consist of the smallest geo graphical soil areas convergent to the taxonomic units of soil classific ation. They are called by F r i d 1 a n d [4] the elementary soil areas (EOG). Their basic feature should be the profile homogeneity on a deter mined unit of the surface and the complexity in space connected with the formation of the relief. The problem of both homogeneity and complexity of the features connected with the relief is the subject of the present paper.
TH E OBJECT A N D M E TH O D S OF R E SE A R C H
The cartographic investigations w ere carried out at the Laska Forest District Administration (Tuchola Forests) in the scale of 1:1000 on the surface area of 16 hectares of a dry pine forest with a 70 to 75 years old stand. This is a fragment of a sander plain of the Brda River trans formed by aeolian processes. It is situated east of glacial channel lakes joined together by the Brda River.
The object is characterized by a great differentiation of relief varying from 127,6 to 145Д metres a.s.l.
218 A. K ow alkow ski, J. Borzyszkowski
The more important soil properties w ere determined in the samples taken from individual horizons and layers of three soil profiles respec tively. The grain size was determined by both the sive and areometric method after Bouyoucos with Casagrande’s and Prószyński^ modification. The pH was determined by the electrometric method using a glas electro de, and organic С by Tiurin’s method. On individual elements of the relief medium samples w ere taken from the FH, A E , Ih and If horizons, each time applying their cutting out from micromonoliths with a simul taneous measurement of their thickness. In the samples p H KCi was de termined, while in 0.03 C H 3C O O H extract— readily soluble forms of Ca, Mg, К and P. The interpretation of results of investigations was carried out in the F H horizon features of which were direct indicators of the influence of a surrounding environment on the formation of soils.
R E S U LT S OF IN V E S T IG A T IO N S
The area investigated has been morphometrically differentiated on a highly elevated embankment oriented SSE— N N W . It passes in the S W direction into a depression of the channel type at a depth of 20 metres, and in the N E direction into a flat depression of the basin type at a depth of 23 metres. The whole object is composed of medium and coarse-grained sands. The sands 40 to 50 cm thick in the surface layer are devoid of sedimentation structures. A gravel-stone horizon exhibiting the features typical of the periglacial genesis is present in the floor of this layer.
The results of analysis of the grain size (Table 1) indicate that fractions > 0 .1 mm are considerably differentiated. In a given locality, especially in a flat valley, the fraction content > 1 .0 mm accounts for 20 to 30 percent in relation to the whole mineral soil mass. These sands gave rise to autogenic rusty podzolic soils with a profile L -F H -A E - -I h -B v -B V C -C .
They developed under conditions of a markedly differentiated meso- relief and of a washed type of water management.
Despite relatively great differences in the organic carbon content in the F H and A E horizons (Table 1) the cover of rusty .podzolic soils is distinguished by a high continuity of welldeveloped genetic horizons. According to B i e ł o b r o w and F r i d l a n d [1] this is therefore a parallel to the homogeneous elementary soil area (H EO G ). Attention should be draw n to the lack on that area of toposequences of rusty podzolic and podzolic soils developed from fluvioglacial and aeolian sands that are commonly encountered in Central Europe.
T a b l e 1
Grain size and. some chemical properties of soil
Horizon
Fraction content in per cent
С % Ą c i > 2 0 mm 20—2 mm
2 - 1
mm 1-0.5 шт 0.5-0.25 mm 0.25-0 .1 mm0 . 1 — 0 . 0 2 m m
< 0.02 mm FH 26.92-42.14 54.62 2.6-5.0 AE0
0.4-1.60 . 8
2.1-11.55.2 18.0-37.0 26.0 29.0-37.0 I3.O-3O.O 5.0-9.0 5.0-5.0 0.86-1.49 5 .0-5 .7 33.3 23.7 7.0 4.0 1.09 Ih0
0.5-1.91 . 2
3 . 8 - 1 1 . 8
7.83 0 . 0 - 3 6 . 0
33.0 28.0-35.0 31.61 1 . 0 - 2 0 . 0
I5.6 6.7-6.96 . 8
5.8-4.5 4.0 0.60-0.770 . 6 8
5 .8-4.0 Bv 0 0.4-6.5 2.4-15.0 12.6-42.0 20.0-34.0 9. О -
45. О
5.0-6.0 2.0-2.4 0.58-0.42 4.0-4.1 2.5 7.3 28.5 28.0 26.0 5.7 2.1 0.59 BvC 0 0.3-5.7 2.5 2.7-24.0 10.6 15.0-47.0 32.1I
9. O -
39. O
30.3 2.O-35.O 20.0 1.5-6.0 5.0 1.0-2.0 1.5 0.03-0.06 0.046 4.6—4.7 С/Сд/ 0 0-2.8 0-16.1 7.0-41.0 52.0-35.5 2.5-57.О 2.5-4.0 1-2.5 0.01-0.02 4.
8-
5.0 0.965 . 8
19.7 33.4 35.2 5.21 . 8
0.02 d/c2/ 0 2.7-3.2 2.9 6.1-8.1 7.1 53.0-60.0 18.О-ЗО.О 5.0-10.0 1.8-1.8 1-2 0.01 4.7-5.0 56.22 4 . 0
6.5 1.8 1.5 to »-* CD R e s e a rc h on th e rev e rs e c o u p li n g s ...2 2 0 A. Kow alkow ski, J. Borzyszkowski
The homogeneous soil cover exhibits a distinct qualitative and quan titative differentiation in space of individual genetic horizons which have developed due to the existing inclinations and specific geochemical couplings involved. A long-lasting migration of elements has bound together all elements of the relief as w ell as all incorporated soils and plant associations into one reverse coupled system. The parent rook and the type of water management have decided, however, on the homo geneity of soils.
U g g l a a n d F e r c z y ń s k a [7] a also F e r c z y ń s k a alone [2] call attention to the indicator value of raw humus in the catenas of forest habitats. The authors point out to the fact that the thickness of the F H horizon in these habitats is dependent on the depth of ground water table and on the composition of species in plant associations.
Research on the reverse couplings... 221
Fig. 2. The form ation of p H Kci in the F H horizon
On the analyzed area the studies on the thickness of the F H horizon, of its p H KCi and readily soluble compounds contained there in do not confirm a too far-reaching generalization raised by mentioned authors. Interdependence between the depth of the ground water table and the amount and quality of ra w humus is in the case of precipitation-ground water management commonly known. Under conditions of water mana gement of a washed type only, there should exist independent, separate regularities of the formation of the F H horizon with humus of xeromor type. This problem w ill be considered on an example of detailed carto graphic materials as shown in Fig. 1-6.
The thickness of the F H horizon varies between 3 to over
6
cm, irrespective of the soil moisture. Characteristic is the greatest thickness amounting to more than6
cm on the top part of the embankment, the222 A. K ow alkow ski, J. Borzyszkowski
lower parts of its slopes and the close-by glacial channel. On the other hand a flat basin is distinguished by the lowest thickness of that horizon amounting to about 3 cm (Fig.
1
). The tendencies toward a decreasing thickness of the F H horizon also occur in the upper parts of the embank ment slope. The reaction ranging from p H 2.7 to 3.0 w ell correlates withFig. 3. The content of readily soluble calcium (Ca) in mg/100 g of soil in the F H horizon
the ascertained soil pattern which by no means limits the continuity and genetic homogeneity o f the rusty podzolic soils investigated. A s Shown in Fig. 2 the higher p H values are correlated w ith the F H horizon of a greater thickness, and acidity increases as raw humus decreases. This confirms the separateness of the catena as compared to the toposequence
Research on the reverse couplings... 223
Fig. 4. The content of readily soluble magnesium (M g) in mg/100 g of soil in the
FH horizon
characterized by U ggla and Ferczyńska. Fhe content of readily soluble Ca (Fig. 3) confirms the regularity of soil pattern defined b y the thickness of the F H horizon and its pH. A t the same time the presence of this element distinctly refers to the morphometry of the earth’s sur face. Less distinct are the quantitative relations of Mg, even though that they still refer to the asserted regularity (Fig. 4). On the other hand readily .soluble phosphorus the amounts of which decrease with the in creasing mass of the F H horizon and its decreasing acidity shows the tendency in inverse proportionality (Fig. 5). The exception is a flat basin w here phosphorus also occurs in minimum quantities. Separate regulari ties are observed in the quantitative relations of readily soluble potassium the greatest amounts of which w ere found on the slope oriented NE,
224 A. Kow alkow ski, J. Borzyszkowski
small— on the slope oriented S W and the smallest in a flat basin (Fig.
6
). From section A -В cut through the area at a length of 360 m in the S W — N E direction (Fig. 7) w e have found that each of the three forms of the mesorelief investigated constitutes a separate subunit H E O G withFig. 5. The content of readily soluble phosphorus (P ) in mg/100 g of soil in the
F H horizon
a specific system of features differing from those found in the adjoining subunits. A s it is, the low er surfaces of slopes and the embankent ridge are characterized by the F H horizon of a greater thickness and the higher values of pH, Ca and Mg.
On the contrary, P and К exhibit an individual quantitative system. In the upper parts of slopes there are tendencies toward a decrease in
Research on the reverse couplings... 2 2 5
the quantitative relation of the soil features except for P and K. A flat basin distinguishes itself in turn by minimum quantities of all features of the F H horizon, whereas in a narrow and deep depression of the glacial channel, the majority of such features attain their maximum. Hence, w e infer that in such depressions a spatial system of individual features
Fig. 6. The content of readily soluble potassium (K ) in mg/100 g o f soil in the
F H horizon. Section A -В through the terrain investigated
depends on the magnitude of their forms. In the case of a glacial channel the dominant effect was imposed on its specific features by the action of the geochemical coupling of the lower part of slops of the surrounding embankments. In the case of a flat basin, its surface and the grain size of parent rock have decided on the separability and development of pedogenic features.
226 A. K ow alkow ski, J. Borzyszkowski 0 100 200 300 f e i i 1 j1 I I 11 i I 1 r 5 ! i £ ! S l c i i C l 1 ^ i ^ i 1 ^ 1 ^ i f a l l f I g 1 1 ^ ' ^ § 1 i ! i i i i
1
1 ^
1 §
I ё £ 1 ^ 1 ■ f e 1 l | < 5 1 1 ! | | J / ^ i ■ S 3 ® I o i Cû ! ъз Г £ г 1 c -j 1 C o 1 C o 1 slopeII
C o 1 1 4 ^ 11 !
- 8 . 1 slo pe FH Horizon ReliefFig. 7. R eciprocal couplings between the m orphom etrical elements of the earth’s surface and some features of the F H horizon in section A — В
S U M M A R Y
A cartographic elaboration at the scale of 1:1000 has enabled to single out within the compass of (H EO G ) the subunits of the surface distinguished b y the diagnostic features of the F H horizon which have developed due to specific geochemical couplings associated with the morphology of the earth’s surface. There is a distinct linear distribution of phenomena of anisotropic character, the boundaries o f which occur in the zones of the geochemical incompatibility often localized in places of the change in the inclination of the earth’s surface. A n individual complex of areas with the reciprocally coupled features of the F H horizons has developed on each of the forms of the relief investigated. Such horizons are not, however, so specific that they should cause dis continuity in the HEOG. The taxonomic values of these features are
Research on the reverse couplings... 227
lower than the subtype of the soil viewed from the area angle. They have, however, an indicatory pedogenic value. They refer in a sense to the soil individual and each of the areas corresponds to the polypedon in K o z ł o w s k i’s sense [6]. Owing to the association of this unit with the relief one suggests that it can be called topopolypedon. The complex of these units forms the toposequence of polypedons bound with a given unit of the earth's surface. Further studies are under way.
REFERENCES
[1] B i e ł b r o w W. P., F r i d l a n d W. M.: Opyt koliczestwiennoj charaktieristiki m orfologii elementarnych poczwiennych arieałow i słoistosti poczwiennogo po-krowa. Zakonom iernosti prostranstwiennogo w arirow an ija sw ojstw poczw i in- form acjonno-statisticzeskije m ietody ich izuczenija. M oskw a 1970, 5-14.
[2] F e r c z y ń s k a Z.: M orfologia i odczyn próchnicy nakładowej w katenie sie dlisk borowych. Zesz. nauk W S R Olszt. 25, 710, 739-747.
[3] F i n k J.: Bodensekwenz in Österreich. 8th Int. Cong. Soil Sei., Bukareszt 1964, 741-750.
[4] F r i d l a n d W. M.: Elem ientarnyje poczw iennyje areały как ischodnyje jed i- nicy poczw ienno-gieograficzeskoj taksonomii i n iekotoryje ich proizw odnyje. Zakonom iernosti prostranstwiennogo w arirow an ija sw ojstw poczw i inform a- cojnno-statisticzeskiej m ietody ich izuczenija. M oskwa 1970, 5-14.
[5] K o p p D.: W iederspiegelung des Grundwassers und der Staunässe in der K lassifikation der Bodenform en und Bodenmosaike am Beispiel der W a ld böden des Tieflandes. Arch. Forstwesen. 19, 28, 843-851.
[6] K o z ł о w s k i F. I.: Poczw ien n yj inwiduum i m ietody je jo opredielenija. Z a konomiernosti prostranstwiennogo w arirow an ija sw ojstw poczw i inform aejon- n o-statisticzeskije m ietody ich izuczenija. M oskwa 1970, 42-59.
[7] U g g l a H., F e r c z y ń s k a Z.: Stosunki glebow e w katonie siedlisk borowych „K u d y p y ” . Zesz. nauk. W S R Olszt. 25, 1969, 709, 719-732.
А . К О В А Л Ь К О В С К И , Я. Б О Ж И Ш К О В С К И И С С Л Е Д О В А Н И Я П О О Б Р А Т Н Ы М С О П Р Я Ж Е Н И Я М М Е З О Р Е Л Ь Е Ф А И Н Е К О Т О Р Ы Х С В О Й С ТВ Г О Р И З О Н Т А F H О П О Д З О Л Е Н Н О Й Р Ж А В О Й П О Ч В Ы О тдел почвоведения и удобрения Н аучно-исследовательский институт лесного хозяйства Опытный центр Сэнкоцин Р е з ю м е Подробная картографическая разработка в масштабе 1:1000 п озв оли ла в ы дели ть в пределах гомогенных элементарных почвенны х ареалов (Э П А ) подъ- единиц площ ади различаю щ иеся по диагнозическим свойствам почвенного го
228 A. K ow alkow ski, J. Borzyszkowski ризонта FH , образованных вследствие специфических геохимических сопря жений, связанны х с м орфологией поверхности земли. В данном случае про изош ло линейное размещение явлений с признаками анизотропности пределы которы х обозначаются в зонах геохимических несогласий локали зую щ и хся ч а сто в местах изменения уклона поверхности земли. Н а каждой из исследуем ы х форм рельеф а образовался специфический различны й комплекс почвенны х площ адей с взаимно сопряженными свойствами горизонтов FH , которые, одна ко, не на столько различны, чтобы вы звать непостоянства в Э П А . Таксоно мические величины этих свойств ниже подтипа почвы в пространственном от ношении, однако они имеют показательную педогенетическую ценность и в и з вестном смысле показываюат увязк у с почвенным индивидуумом, а отдельны е площ ади отвечают полипедону в см ы сле К о з л о в с к о г о [6]. Ввиду связи этой единицы с рельеф ом предлагается назвать ее топополипедоном. К ом плекс этих единиц составляет топосеквенцию топополипедонов связанную с данной единицей поверхности земли. И сследования продолжаются. A . K O W A L K O W S K I, J. B O R Z Y S Z K O W S K I
ETUD ES SUR LES C O N T R E R É A C T IO N S E N T R E U N M É S O R E LIE F E T Q U ELQ U ES P R O P R IÉ T É S DE L ’H O R IZ O N F H D ’U N S O L OCHRE
P O D Z O L IQ U E
D épartem ent de Pédologie et de Fertilisation Institut des Recherches Forestières à Sękocin
R é s u m é
Une interprétation e ffe c tiv e d’un p ro fil du sol ne peut se réaliser uniquement par la connaissance nette des causes de son développement. I l faut le regarder comme le résultat de l ’interaction de tous les facteurs présents du milieu.
L ’objet de nos recherches a été un sol ochre podzolique provenant des sables éoliquem ent transformés et sous une fo rêt de pin de 70 ans. Les résultats des analyses granulométriques, du pH au KC1 ett de la teneur en carbone se trouvent sur le tableau 1, tandis que les graphiques 1-6 représentent les teneurs en Ca, Mg, P et К solubles dans 0,3n CH3COOH de l ’horizon F H du sol.
Une élaboration cartographique détaillée à l ’échelle 1 :1000 a rendu possible l ’isolement, au sein des territoires — rayons homogènes élémentaires, des sous- éléments séparés rem arquables par leurs traits diagnostiques à l ’horizon F H et dont les lim ites s’accordent en général avec celles des conform ités géochimiques et avec l ’inclination du terrain.
Les valeurs taxonomiques de ces sousélément se placent au dessous du soustype du sol. On peut les regarder pourtant comme indices pédogénétiques correspondant aux polipédons de K o z ł o w s k i [6]. On propose de les appeler topopolipédons vue leur conform ité au relief. L ’ensemble de ces éléments form e une toposéquence des topopolipédons liée avec l ’unité de la surface de terre.
Research on the reverse couplings... 229
A . K O W A L K O W S K I , J. B O R Z Y S Z K O W S K I
U N T E R S U C H U N G E N Ü B E R R Ü C K K O P P L U N G E N Z W IS C H E N D EM M E S O R E LIE F U N D E IN IG E N E IG E N S C H A F T E N DES F H -H O R IZ O N T E S
IM R O S T P O D S O LIG E N BO D EN
A bteilu n g fü r Bodenkunde und Düngung, Forschungsinstitut, fü r Forstwissenschaften Forschungszentrum Sękocin
Z u s a m m e n f a s s u n g
lin e eingehende K artieru ng im Masstab 1 :1000 hat erm öglicht im homogänen elem entaren Bodengebiet einige Flächenuntereinheiten m it unterschiedlichen d ia gnostischen M erkm alen im F H -H orizon t auszusondern, die als Ergebniss eigen artiger geochemischer Rückkopplungen verbunden m it der O berflächenm orphologie entstanden sind. Es ist eine klare lineare anisotrophieartige Dislokation der P h ä nomene feststellbar, deren Grenzen in Zonen geochemischer Diskordanzen lo k a li siert sind, und in der R egel m it einem W echsel der Neigung der Erdoberfläche übereinstimmen. Innerhalb jeder der untersuchten R eliefform en ist eine Verge sellschaftung der Flächeneinheiten m it gegenseitig gekoppelten M erkm alen im F H -H orizon t festzustellen, die jedoch nicht so w e it verschieden sind um in dem homogänen elem entaren Bodengebiet Diskordanzen zu verursachen. D er taksono- mische W ert dieser M erkm ale liegt tiefer als der des Bodentyps im Sinne der Oberflächeneinheit Er ist doch ein pedogenetischer W eiser, der dem B oden in divi duum nahe steht. Is Sinne K o z ł o w s k i s [6] jeder dieser Flächeneinheiten ent spricht der Polipedon, m it dem R e lie f verbunden als Topopolipedon benannt. Eine Assoziation dieser Einheiten verbunden m it einer gegebenen Oberflächeneinheit w ird als seine Toposekwenz der Topopolipedone angesprochen. W eitere U n ter suchungen w erden durchgeführt.
A . K O W A L K O W S K I , J. B O R Z Y S Z K O W S K I
B A D A N IA N A D Z W R O T N Y M I S P R Z Ę Ż E N IA M I M IĘ D Z Y M E Z O R E L IE F E M A N IE K T Ó R Y M I W Ł A Ś C IW O Ś C IA M I P O Z IO M U F H
G L E B Y R D Z A W E J B IE L IC O W A N E J Zakład G leboznawstwa i Nawożenia,
Instytut Badaw czy Leśnictwa, Ośrodek B adaw czy w Sękocinie
S t r e s z c z e n i e
Odpowiednia interpretacja profilu glebow ego nie może być osiągnięta przez poznanie jedynie przyczyn praw idłow ości jego rozwoju. C elow e jest rozpatryw anie jego cech jako w yniku in terakcji wszystkich czynników środowiska oraz przystoso w ania do danego środowiska. Historia gleb w danym środowisku jest odzw iercie dlona w ich sekwencjach, których dokładne rozpoznanie może nastąpić przy za stosowaniu w ielkoskalow ej k artografii uw zględniającej cechy krajobrazow e. Badania przeprowadzono na pow ierzchni 16 ha w nadleśnictwie Laska (B ory Tucholskie). W obiekcie badawczym pod 70-75-letnim drzewostanem sosnowym w ystępują gleby rdzaw e bielicowane, w ytw orzon e z piasków sandru B rdy eolicznie przekształconych.
230 A. K ow alkow ski, J. Borzyszkowski
czeń w w yciągu 0,03n CH3COOH łatw o rozpuszczalnych form Ca, M g, P i К w p o ziom ie F H przedstawiono graficzn ie na rysunkach 1-6.
Szczegółowe opracowanie kartograficzne w skali 1 :1000 um ożliw iło w y d z ie lenie w obrębie homogenicznych elementarnych obszarów glebow ych (H EO G ) pod- jednostek powierzchni, różniących się cechami diagnostycznym i poziomu glebow ego
FH , pow stałym i wskutek swoistych sprzężeń geochemicznych związanych z m o rfo
logią powierzchni ziemi.
W ystąpiło tu w yraźnie lin iow e rozm ieszczenie zjaw isk o cechach anizotropo- wości, których granice powstają w strefach niezgodności geochemicznej, lokalizu jących się często w miejscach zm iany nachylenia powierzchni ziemi. Na każdej z badanych form reliefu w y tw o rzy ł się swoisty, odrębny zespół obszarów z w z a jem nie sprzężonym i cechami poziom ów FH , które jednak nie są tak dalece odrębne, aby pow odow ały nieciągłość w HEOG. W artości taksonomiczne tych cech są niższe od podtypu gleby w sensie obszarowym, m ają jednak w skaźnikową wartość pedo- genetyczną i w pew nym sensie nawiązują do indywiduum glebowego, a każdy z ob szarów odpowiada polipedonow i w sensie K o z ł o w s k i e g o [6].
Ze w zględu na powiązania tej jednostki z reliefem proponuje się nazwanie jej topopolipedonem. Zespół tych jednostek tw orzy toposekwencję topopolipedonów związaną z daną jednostką powierzchni ziemi. Dalsze badania w toku.
Doc. d r h a b. A l o j z y K o w a lk o w s k i Z a k ła d G le b o z n a w s t w a i N a w o ż e n ia In s ty t u tu B a d a w c z e g o L e ś n ic tw a O ś r o d e k B a d a w c z y w S ę k o c in ie
