Zagadnienie typologii gleb kopalnych na przykładzie Nieledwi

R O C Z N I K I G L E B O Z N A W C Z E , T . X I X , D O D A T E K , W A R S Z A W A 1968

K R Y ST Y N A K O N E C K A -B E T L E Y

TH E TY PO LO G Y O F FO S S IL SO ILS ON TH E EX A M PLE O F N IELED EW

L aboratory of th e C h em istry and P h y sic s of S oils In stitu te of S o il S c ie n c e and P la n t C u ltiv a tio n , W arszaw a

The stra tig ra p h y of th e loess of th e L u b lin U plands h a d been w ork ed out fro m its m an y angles b y m any au th o rs. S tra tig ra p h ie w ork from various po in ts of view th ro w s a lig h t on th e process of th e fo rm atio n of loess an d also enables to d e te rm in e an d ch aracterize th e fossil soils of th ese areas [3, 5, 7, 8, 10, 11, 14].

The objective set in th e p re se n t w ork, b ased on Ró ż у с к i ’ s s tr a ti­ g rap h ie schem e [12], w as to d e te rm in e th e course of th e soil-form ing process in each of th e phases of fossil soil fo rm atio n, not only on th e basis of m orphological fe a tu re s b u t also on c e rtain ph ysico-chem ical c h a ra c te ­ ristics.

A closer in sig h t in to th e essence of soil-form ing processes req u ires p ay in g a tte n tio n to th e evolu tio n of soils, w hich as reg a rd s to fossil soils is fre q u e n tly c o n tro v ersially tre a te d [7, 8, 10, 11].

The changes tak in g place in soils d ep end on th e w hole of th e so il-fo r­ m ing facto rs am ong w hich a larg e role is p lay ed by th e len g th of th e period of soil-fo rm ation [1, 2, 4, 6, 9, 13].

The profile in N ieledew (H rubieszów county), w as selected for in v esti­ gations owing to th e larg e role th a t it p lay s in th e d e te rm in a tio n of th e loess stra tig ra p h y of th e L u b lin U plands, for, th re e fossil soils occur in th is profile — th e oldest — in te rg la c ia l an d tw o y o un ger, m ost prob ably in te rsta d ia l [8].

On th e basis of th e m orphological fe a tu re s d ete rm in e d and of th e re su lts of an aly ses (Tab. 1, 2) th e follow ing fossil soils of N ieledew can

Some p h y sic o -c h e m ic a l p r o p e r tie s o f in v e s tig a te d s o i l T a b l e 1 Samples No. Horizon PH CaCO}

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Leached chernozem, l e s s i v e chernozem - f o s ß i l s o i l II

X _A1 6 . 9 7 .5 1.89 2 . 5 0 14 .6 5 12.15 8 2 . 9 2 7 . 9 0 . 8 5 2 .3 0 0 . 2 6 0. 0 43 4 _6.0 XI ₄ 6 . 9 7 . 6 2.1 0 1. 50 1 3 .1 8 1 1 .6 8 8 8 .6 1 5 .7 0. 9 5 3 . 0 2 1.14 0. 08 03 1 4 . 1 XII A]B 6 . 9 7 . 6 0. 84 0 .0 1 2 . 8 2 12:82 1 0 0 .0 2 8 . 0 1 .0 0 3 . 7 2 0 . 2 7 0. 0 41 3 6.1 XIII В 6.8 7 . 6 1.17 0 . 2 5 1 5 .8 1 15 .5 6 98 .3 4 0 . 0 1.7 0 4 . 3 6 0 .1 2 0.0 1 57 7 . 6 XIV С 6 . 9 7 .4 0 . 7 1 0 .0 11 .7 3 11.73 1 0 0 .0 5 3 . 8 1 .2 0 3 .2 5 n .o . n .o . n .o . XV CG 6 . 9 7 . 5 0 .0 4 . 1 3 7. 8 3 3 .7 0 4 7 . 2 5 3 . 8 1 .2 0 3. 2 0 n .o . n .o . n .o . Leached brown s o i l - f o s s i l s o i l I XVI _A1 6 . 9 7 .5 0. 33 3 . 7 5 4 . 1 5 0 . 4 0 96 .3 5 3 . 8 0.61 2 .3 0 0 . 1 9 0.0212 9 . 0 XVII B(B) 6 . 9 7 .3 0 .2 1 2 . 5 0 9 . 3 1 6 . 8 1 73 .0 63.6 1. 1 5 3 . 1 0 0 . 2 7 0.0226 1 1 .8 XVIII С 6 .8 7 . 5 0.3 3 4 . 0 0 9 . 4 9 5 . 4 9 5 7 . 8 4 0 . 0 1. 18 1.2 7 n . o . n . o . n . o . K o n e c k a -B e tl e y

The ty p o lo g ie of fo s s il soils 263 T e L 1 e 2 M e c h a n ic a l c o m p o s i t i o n in p e r c e n t Samples No. 1 -0 .1 0 . 1 - 0 . Op _{0 .0 2}0 . 0p- 0 . 0^.-_{0 .0 0 b} O.üCb-_{0 .0 0 2 !}< 0 . 0 0 2 T o ta l i - o . i ; 0 .1 - 0 .0 3 < 0 . 0 0 2 miii " T ip ic a i" chernozem - r e l i c ■ t s o i l 1 3 3 46 27 ! ! 7 1 ! 14 ii _{1 ^} , i_{! 49} 48 II 4 8 42 2o j s ić 4 i 30 46 I I I s 9 40 23 9 10 ? ! 49 44 IV 2 10 43 29 ! 6 ! 5 2 ; 33 43 V 3 9 37 30 ! i i 1 10 3 4b 31 VI 1 b 10 32 28 _{! 15 1 11 i} с !₁ 42 32 E rodet l e s s i v e s o i l - î ' o s s i l s o i l I I I VII 7 8 40 ‘-0-j i i s 12 7 48 43 V III 9 10 42 20 ! ô 10 9 :>2 39 IX 10 10 39 23 i i 1 10 i i i 1 49 41

Leached chern ozeb, l e s s i v e chernozem - f o s s i . 1 s e i l II 1 . ! a a . 0 1 1 29 1_{! 1 2} , 8 !...38 i 34 ' XI ! 7 9 3o i 33 ₆ 7 i 7 43 48 XII 7 3 34 ! 25 i i 7 43 ! ^0 X III - 10 9 21 34 8 ; 12 10 3o 34 XIV ! i з i 7 34 _{! 31} i 18 _{' 3} 3 41 i ' • 4 Leached Drown sc i l - l o s s i .1 s o i l I j XVI 9 1 8 1 39 i 23 i 9 ! i 7 1 _I ! 4 7 I I 44 ; XVII 7 b 35 27 12 _{! ^} 7 41 32 XVI11 7 i 0 i « i 23 ! 14 ! i L . . * 7 j 48 i 1 4b.

T he process of th e fo rm atio n of th e oldest soil should be re fe rre d to th e Eem s in te rg la c ia l period (Riss) W ürm J. III (IV opt. int.) n o tin g th a t th e soil-loess m a te ria l w as deposited to w a rd th e decline of Riss.

T he genetic horizon in d icates a leach ed bro w n soil. H orizon A, of sm all dep th , does n o t contain m uch h um us. Below th is horizon is m ark ed horizon В (В) — underg oin g a brow ing process, to g eth e r w ith th e sub h o ­ rizon of w ash ed out ferro u s com pounds, as in d icated by th e re su lts of analyses. It is p rim a rily en rich ed in its to ta l c o n ten t as w ell as in th e free form of th is com ponent. A c e rta in e n ric h m e n t in colloidal p a rts is also to be n o ted in th is horizon an d in its u p p er p a rt — a c e rtain accu m u­ latio n of organic com pounds. W ith such a c o n ten t of carb o n ates in th e loess m a te ria l th is cannot be ex p lain ed as being a leaching of hu m us com pounds in th e fo rm of com plex com pounds; it should r a th e r be

234 K. K o n e c k a -B e tle y

tre a te d as a relict subhorizon of fo rm er chernozem soil. This observation enables to d raw th e conclusion th a t m ost p ro b ab ly a chernozem re la tiv e ly w eak ly developed w as form ed in th e firs t place in fo rest-step p e conditions from soil w eak ly developed fro m c arb o n ate loess d u rin g th e Eem s in te r ­ glacial period. In consequence of th e changes of vegetatio n al-clim atic conditions of v eg etatio n succession, th e re w as overlain th e process of b row ning and th e n in consequence of f u rth e r changes of th e phy sico -ch e­ m ical conditions — th e leaching out of carb o n ate com pounds, th e re w as form ed a bro w n leached soil.

The w ay th e soil form ing process took place not only does not in d ic a ­ te podzolization, b u t even a lessivage is n o t v e ry probable. W ith such a high degree of basic sa tu ra tio n , soil-form ing ceased m a in ly w ith th e dis­ p lacem en t of easily soluble salts an d only to a sm all degree w ith iro n com ­ pounds. U n d er such ph y sico-chem ical conditions w ith such a high pH an d w ith a c e rtain carb o n ate conten t, th e re can be no question of alum ino sili- cate decom position an d disp lacem en t of th e pro d u cts of th e ir decom posi­ tion w hich is a c h a ra c te ristic fe a tu re of th e podzolization process. F rom th e point of view of physico-chem ical p ro p erties, it does not seem th a t conife­ rous forests p red o m in ated d u rin g th e last phase of th e Eem s in te rg la c ia l period, b u t coniferous tre e s m ig h t have occu rred in a m ix tu re and m ight have been of sh o rt d uratio n .

The gley horizon, o v erlying horizon А г of Eems soil, is connected w ith th e in itia l phase of loess W ürm sed im en tatio n , a lre ad y u n d e r th e condi­ tions of an A rctic clim ate. The lay e r of th is gleyed loess, of o th er sed im en ­ tatio n , m ig h t have e x e rte d to a c ertain degree an in flu en ce on certain physico-chem ical p ro p ertie s such as ac tiv atin g c e rtain com ponents in low er lying soils.

The fossil soil n e x t in order, fo rm ed over the Eem s in te rg la c ia l soil is a chernozem leached chernozem lessive (brunizem ), form ed from c a r­ b o nate in te rsta d ia l loess (Göttw eig) G IV -2/-1. This soil is c h aracterized by th e follow ing genetic horizons: H orizon A x w eak ly h u m u m of g ray colour, A \ a horizon of a g re a te r h u m u s content, d ark g rey in colour w ith a violet tin t, horizon А г В of a sm aller h u m u s conten t, lig h t g ray -b ro w n horizon B, illuv ial, lig h t brow n in colour, С m a trix rock light yellow , CG m a trix rock horizon, ra th e r th ick w ith g ray -b lu e gley m ottles. T he above m orphological fea tu re s, passing into the d ep th of th e profile fro m the A 1 horizon, and th e re su lts of an alyses in d icate a c e rtain leaching of the ferro u s com pounds an d also to a low degree of clay p a rts (w ithout th e ir decom position) in d icatin g the p rin cip al sh are of steppe v egetatio n in the firs t phase, a r a th e r rap id phase of th e fo rm atio n of th is soil, an d in th e second phase — of fo rest-step p e p a rk v egetation.

The ty p o lo g ie of fo s s il so ils 265

It m ay be supposed th a t th e soils fo rm ed c o n stitu te an in te rm e d ia te stage b etw een chernozem and fo rest sierozem s. The la tte r a re form ed w ith a g re a te r sh are of coniferous fo rest v eg etatio n and are ch a ra c te riz e d by a low er degree of base cation sa tu ra tio n as com pared w ith brunizem s. N ote also th a t w h a t are called b ro w n ed chernozem s, also occur contem ­ p o ran eo u sly on these areas, being form ed in h u m id clim atic conditions, w hich m ost p ro b ab ly did not p rev a il in th a t period.

The alm ost tw o -fo ld increase in easily soluble form s of ferro u s com po­ u n d s — w h a t are called free in horizon В — in d icates lessivage in condi­ tion s of a w arm , re la tiv e ly m oist clim ate, w ith a sm aller sh are of x eroph illo u s p la n t species. The d isplacem en t of free ferro u s com pounds in w eak ly alk ali conditions in dicates a periodic anaerobiosis, w hich in conditions of considerable h u m id ity w as caused by th e red u c tio n of iron to a b iv ale n t form . A c e rtain co n ten t of carb o n ates in th e m a trix rock, ex pressed in a high degree of basic sa tu ra tio n , e x e rte d u n q u estio n ab le in flu en ce on th e accu m u latio n of calcim orphous hum us, w hich in tu rn w as decisive as reg a rd s th e sta b ility of th is soil.

N ev erth eless, even w h en th e reactio n w as slig h tly alkalin e, th e basic com pounds w ere leached out an d a c e rtain leaching out of ferro u s com ­ p ounds took place, as depen ding on th e clim ate. In those conditions, th e re w as also a m ark e d m in eralizatio n of organic substances.

A ll th e fe a tu re s m en tio n ed above in d ic a te th a t th e period of fo rm atio n of th is soil in th e in te rsta d ia l period w as re la tiv e ly sh o rte r w h en com pared w ith th e Eem s in te rg la c ia l soil and th a t its typology w as m ore stab le as dependin g on th e m in e ral com position of th e soil m a te ria l (more calcium carbonate).

The lig ht g ray horizon А 'ъ o v erlying horizon A x tak in g into co n sid era­ tion its m ech anical com position, m ay b e a r testim o n y to th e fact th a t a new loess facies m ig h t have been blow n at th e decline of G IV -2/-1 on an a lre a d y w ell-developed hu m u s horizon.

The y o u ng est fossil soil w as form ed from y o unger W ürm loess w ith o u t c arb o n ate in th e G IV-1 P a u d o rf in te rsta d ia l period, according to Różycki. Above all, stress m u st be laid on th e specific conditions of sed im en tatio n of loess on leached chernozem . The stra tific a tio n occurrin g in th is m a te ria l (about 70 cm) m ost pro b ab ly in d icates an A eolian deposition of loess in a w a te r reserv o ir, w hich is connected w ith th e physico-chem ical p ro p ertie s of th is m aterial. The u p p er lay ers of th e loess of th is facies do not d isp lay stra tific a tio n . T aking th e e n tire soil pro file into account, note th a t it is sh o rte r in consequence of erosion.

266 K. K o n e c k a -B e tle y

It m ay be supposed th a t d u rin g th is period brow n soil w as form ed, w h ich in consequence of th e basic com pounds being leached, gave w ay to th e lessivage process and n ex t, in consequence of th e top horizons being cleared off, a soil w as form ed w ith a d elu v ial h um us horizon d ire c tly o v erlying th e illu v ia l horizon of B lessivage soil.

The above is estab lish ed n o t only by th e m orphological fea tu re s b u t also by th e re su lts of th e p hysico-chem ical an alyses as: a considerably sm aller d egree of s a tu ra tio n of th e u p p er lay e r as com pared w ith th e d elu v ial horizon an d w ith th e m a trix rock horizon, a low er pH, an d also th e displacem en t of iron to th e В horizon. N ote p a rtic u la rly , th e absence of C a C 0 3 th ro u g h o u t th e e n tire p rofile, w hich m ay have c o n trib u te d to a poor accu m u latio n of hu m u s com pounds an d a m ore rap id process of soil evolution. As depen d ing on th e so il-form ing processes, th e succession of p la n t groups also u n d e rw e n t evolution: a m ixed forest w ith a large coniferous a d m ix tu re m ost p ro b ab ly w as p red o m in an t d u rin g th e fin a l phase of th e form atio n of th is soil.

The y o u n g est fossil soil is o v erlain by a th ick loess of th e you n gest W ürm sed im en tatio n w ith a co nsiderable carb on ate (up to 15 p erc e n t C a C 0 3) co n ten t w hich fact casts a lig h t on th e specific conditions u n d e r w hich th e loess se ttle d on th is area an d on th e in itia l m a te ria l of th e soil form ed. These soils should be classified as th e “ty p ic a l” chernozem s a fte r th e P olish Soil Science Society C lassification (th at m eans u n d eg rad ed chernozem s). No g re a te r d isp lacem en t of ferro u s com pounds w as a sc e rta ­ ined w ith such a large co n ten t of calcium carb o n ate, w hich is ex p lain ed by th e h ig h er degree of sa tu ra tio n w ith basic cations. T he low co n ten t of h u m u s com pounds in th is profile as com pared w ith ty p ical chernozem s (m eadow -steppe zones) in d icates th a t th ey w ere form ed in a fo rest-step p e veg etatio n -clim atic zone, w hich in c e rtain cases leads to th e form atio n of chernozem s poor in h um us.

T hey occur in com plexes w ith leached chernozem s (brunizem s) and w ith gray fo rest soils.

The conditions of th e fo rm atio n of chernozem s on th ese areas should m ost pro b ab ly be associated w ith a fo rest-step p e zone. The develo pm ent of these soils a fte r th e A rctic and p reb o re a l period m ight have tak e n place d u rin g th e boreal period. On th e o th er h an d , th e changes ten d in g to w a rd a process of leaching or brow ning are associated w ith a w arm , dam p clim ate, of th e A tlan tic u m w h en th e share of deciduous fo rest w as larger. T he n a tu re of th e m a trix rock, rich in carb o n ates influen ced , how ever, to w a rd the stab ilizatio n of th e chernozem process, w hich is reflec ted in

The ty p o lo g ie of fo s s il soils 267

such physico -chem ical p ro p ertie s as: co n ten t of C a C 0 3, th e high degree of basic cation sa tu ra tio n , th e absence of free an d to ta l displacem ent.

H ence, th ese chernozem s, in spite of th e above fea tu re s, are d iv erg en t as reg a rd s th e ir p ro p ertie s from ty p ic a l chernozem s of th e m eadow -steppe zone, fo rm ed in conditions of a c o n tin e n ta l clim ate.

T hese chernozem s, ow ing to th e ir being developed du rin g the boreal period, should be tre a te d as relict soils.

T he pap er show s th a t th e re is a co n tin u ity in th e evolution of soil in a h isto rical evolution, connected in th e first place w ith changes in clim ate an d th e succession of p la n t groups ensuing th erefro m .

R EFEREN CES

[1] B r a n d t n e r F.: J u n g p leisto za n er L oss und fo s s ile B oden in N ied erösterreich . E iszeita lter und G egen w art, 4/5, 1954, s. 73.

[2] F i n k J.: D ie fo s sile n B öd en im ö ste r r e ic h is c h e n L öss. Q uartar 6, 1954, s. 43. [3] G r a b o w s k a - O l s z e w s k a B.: P h y sic o -m e c h a n ic a l p rop erties of loess

fo rm a tio n s of th e n orth ern and n o rth ea stern parts of th e Ś w ięto k rzy sk a loess zone a g a in st th e b ackground of th eir lith o lo g y and stra tig ra p h y and th e co n ­ d ition s of th eir occu ren ce. B iul. G eol. UW , W arszaw a 1965, s. 114.

[4] L i e b е г о t h I.: L o ss-se d im e n ta tio n und B od en b ild u n g w äh ren d des P le is to ­ zäns in S a ch sen . G eologie, 12, H. 2, B erlin 1963, s. 38.

[5] M a l i c k i A.: T he stratigrap h ie v a lu e of the lo ess p ro file in P ik u lic e (near P rzem yśl). A n n a le s UM CS, Sec. B, vo. X V , L u b lin 1961, s. 9.

[6] M a ń k o w s k a В.: S o ils of th e y o u n g er P le isto c e n e in th e v ic in ity of Łódź. A cta G eografica L od zien sis, 22, Łódź. T ow . N auk., Łódź 1966, s. 150.

[7] M о j s к i J. E.: T he stra tig ra p h y of lo e s se s in th e L ow er H u czw a B asin on th e L u b lin H igh lan d . B iul. Inst. G eol., 187, W arszaw a 1965.

[8] M о j s к i J. E.: T he correlation of th e stra tig ra p h ie p ro file of th e lo e sse s of th e G erm an D em ocratic R epublic, P olan d and E uropean P art of th e S o v ie t U nion. K w art. G eolog., 9, z. 3, W yd aw n . G eolog., W arszaw a 1965, s. 14.

[9] M ü с к e n h a u s e n E.: D ie stra tig ra p h isch e G lied eru n g des L o ss-K o m p le x e s v on K arlich im N e u w ie d e r B eck en . Fortschr. G eol. R h ield u. W est., 4, 1959, s. 17. [10] N а к o n i e с z n y S., P o m i a n J., T u r s k i R.: T he con d ition s of th e

occu ren ce of fo s s il soils w ith in th e S zczeb rzeszy ń sk i U pland. A n n a les UM CS, vol. X II, S ectio В, L u b lin 1960, s. 19.

[11] N а к o n i e с z n y S.: S ols fo s sile s dans les lo ess du P la tea u de L ublin. A n n a les UM CS, vol. 15, S ectio B, L u b lin 1961, s. 10.

[12] R ó ż y c k i S. Z.: C iim a tic-stra tig ra p h ic u nits of d iv isio n of th e P leisto cen e. A cta G eologica P olon ica, vol. 14, PW N, W arszaw a 1964, s. 18.

[13] R ó ż y c k i S. Z.: F o ssil alg ea in lo esses. P rzegląd G eolog. 2, W arszaw a 1965. [14] J o in t w ork: S o il m ap of E urope, FAO , B elg ia 1965.

268 K. K o n e c k a -B e tle y

K . K O N E C K A - B E T L E Y

L E PRO BLÈM E DE L A T Y PO LO G IE D ES SO LS FO SSIL E S E N R EL A TIO N AVEC L E PR O FILE DE N IELED EW

I n s t i t u t d ’A g r i c u l t u r e , d e F e r t i l i s a t i o n e t d e P é d o l o g i e , L a b o r a t o i r d e C h i m i e e t P h i s i q u e d e s S o l s à W a r s z a w a

R é s u m é

Ce tra v a il ren ferm e la ca ra ctéristiq u e des sols fo s s ile s d e N ie le d e w (d ép artem en t H ru b ieszów ), fo rm és de dépôts de lo ess. On a adopté la stra tig ra p h ie du lo e ss d ’après Z. B. R óżycki.

La m o rp h o lo g ie et le s p rop riétés p h y sic o -c h im iq u e s des sols fo s s ile s étu d iés dans ce tr a v a il p erm etten t de le s d é fin ir ainsi:

1) Le sol le p lu s a n cien s ’est fo rm é p en d a n t l ’époq u e in terg la cia ire — in tergl. R iss (W ürm I 11 I/I V) opt. int. On p eu t le d éterm in er: sol brun le s siv é .

2) L e d eu x ièm e so l qui e st p lu s je u n e qu e le p récéd en t G IV -2 /-1 s ’est form é p en d a n t l ’in te r sta d ia l G ö ttw eig . C ’e st un ch ern osem le s s iv é (brunizem ).

3) L e tro isièm e so l fo s s ile G IV -1 s ’est form é d urant l ’in te r sta d ia l P audorf. C’est un so l le s s iv é dont le s h orison s su p érieu rs so n t érodés.

A u d essu s du p lu s je u n e so l fo s sile , sur la su rface, s ’est fo rm é un chern osem . C’est un so l re liq u e d’o rig in e a n cien n e. C ette é tu d e n ous m on tre q u ’il fa u t d istin g u e u n e c o n tin u ité d’é v o lu tio n du sol, qui dépend su rto u t de v a ria tio n s du clim a t et d’a sso cia tio n s v é g é ta le s n a tu relles.

K . K O N E C K A - B E T L E Y

D A S PRO BLEM DER TYPO LO G IE V O N F O SSIL E N BÖ D EN A M B E ISPIE L VON N IELED EW

L a b o r a t o r i u m f ü r C h e m i e u n d P h y s i k d e s B o d e n s d e s I n s t i t u t e s f ü r A c k e r b e a r b e i t u n g , D ü n g u n g u n d B o d e n k u n d e i n W a r s z a w a

Z u s a m m e n f a s s u n g

In der A rb eit w ird d ie C h a ra k teristik der aus L öss g eb ild eten fo s sile n B öden in der O rtsch aft N ie le d e w (K reis H ru b ieszów ) erörtert. D ie L ö sstra tig ra p h ie w ar n ach Z. S. R óżyck i an gen om m en . A u f G rund so w o h l m o rp h o lo g isch er als auch m an ch er p h y sik a lisc h c h e m isc h e n B o d e n e ig e n sc h a fte n w u rd en drei fo s s ile B öden abgesondert:

1) D er ä lte ste fo s sile B od en vom In terg la zia l R iss/W ü rm I III/IV opt. int. — a u sg e la u g te B raunerde;

2) D er zw eite, jü n gere B oden G IV /-2/1 (In tersta d ia l G öttw eig) — a u sg ela u g tes T sch ern osjem , T sch ern osjem le s s iv é (B runisjem );

3) D er dritte, jü n g ste fo s s ile B oden G IV -I (In tersta d ia l P audorf) — der B oden le s siv é , m it erod ierten oberen H orizonten.

T he ty p o lo g ie of fo s s il so ils 269

O berhalb dem jü n g sten fo s sile n B od en tritt au f der O b erflä ch e des in der K la ssifik a tio n der P o ln isc h e n B o d en k u n d lich en G e se llsc h a ft als “e c h te ” b ezeic h n ete T sch ern o sjem auf, w e lc h e r a llerd in g s als ein R elik tb o d en zu b etrach ten ist.

In der A rb eit w ird d erau f h in g e w ie se n , dass es im R ah m en der h isto risch en E n tw ic k lu n g e in e K o n tin u itä t der B o d en ev o lu tio n g’ibt, d ie in erster L in ie m it K lim a v erä n d eru n g en und daraus fo lg en d er P fla n zen su k zessio n sä n d eru n g v e r b u n ­ den ist. K . K O N E C K A - B E T L E Y Z A G A D N IE N IE T Y PO L O G II GLEB K O PA L N Y C H N A PR Z Y K Ł A D Z IE N IELE D W I P r a c o w n i a C h e m i i i F i z y k i G l e b , I U N G , W a r s z a w a S t r e s z c z e n i e

P raca za w iera ch a r a k te r y sty k ę g leb k o p a ln y ch N ie le d w i (pow . H ru b ieszów ), w y tw o r z o n y c h z lessu . S tra ty g ra fię le ssu p rzyjęto w g R óżyck iego. N a p o d sta w ie zarów n o m orfo lo g iczn y ch , jak i n iek tó ry ch w ła śc iw o ś c i fizy c z n o -c h e m ic z n y c h gleb rozpoznano trzy g le b y k op aln e. Są to:

— n a jsta rsza g leb a k o p a ln a in terg la cja łu R iss/W ü rm I III/IV opt. int. — gleb a b ru n atn a w y łu g o w a n a ,

— m łod sza g leb a G IV -2/-1 (in tersta d ia łu G öttw eig) — czarn oziem w y łu g o w a n y , czarn oziem le s s iv é (brunziem ),

— n ajm łod sza g leb a k op aln a G IV-1 (in tersta d ia łu Paudorf) — gleb a le s siv é , ze zero d o w a n y m i p oziom am i w ierzch n im i.

N ad n a jm ło d szą gleb ą k op aln ą na p o w ierzch n i w y s tę p u je czarnoziem , w g k la ­ s y fik a c ji P o lsk ieg o T o w a rzy stw a G leb ozn aw czego — „ w ła śc iw y ”, k tó ry uznać n ależy za g leb ę relik to w ą .

P raca w y k a zu je, że is tn ie je cią g ło ść ew o lu c ji g leb y w rozw oju h isto ry czn y m , zw iązan a p rzed e w sz y stk im ze zm ian am i k lim a ty c z n y m i i w y n ik a ją c ą z n ich zm ianą su k c e sji zesp o łó w ro ślin n y ch .

К . К О Н Е Ц К А - Б Е Т Л Е Й П РО БЛ ЕМ А ТИП ОЛО ГИИ И С К О П А Е М Ы Х ПОЧВ Н А ПРИ М ЕРЕ Н ЕЛ ЕДВИ Л а б о р а т о р и я х и м и и и ф и з и к и п о ч в И н с т и т у т а а г р о т е х н и к и , у д о б р е н и я и п о ч в о в е д е н и я в В а р ш а в е Р е з ю м е В тр у д е р ассм атривается хар ак тер и сти к а обр азов ан н ы х из л ёсса и ск о п а е­ м ы х почв в местности Н ел едв я (район Грубеш ув). С тратиграф ию лёсса при н и ­ мали за 3 . С. Р уж и ц к и м . Н а основании как м ор ф ологи ч еск и х так и некоторы х

270 K. K o n e c k a -B e tle y

ф и зи к о -х и м и ч еск и х свойств почв бы ли вы делен ы сл едую щ и е три ископ аем ы е почвы:

— Самая старая и скоп аем ая почва, и н терглац иала R iss/W ü rm I III/IV opt. int. — вы щ елочен ны й бурозём ; — В торая, б ол ее м олодая почва G IV -2/1 (ин терстадиала G öttw eig) — в ы ­ щ елоченны й ч ернозём , ч ер н озём le s s iv é (брунизём ); — Третья, самая м олодая ископ аем ая почва G I V -1 (и н терстадиала Р а и - dorf) — почва le s siv é , с эродированны м и верхн и м и горизонтам и. Н ад самой м олодой ископ аем ой почвой на п ов ер хн ости л еж и т ч ер н озём , оп ределяем ы й в к л асси ф и к ац и и П ольского п очвоведческ ого общ ества как „подлинны й”, которы й однако сл едует считать реликтовой почвой. В тр уде у к азы в ается на сущ ествов ан и е, в р ам к ах исторического р азвити я, п остоянной эволю ции почв, свя занн ой в первую очередь с клим атическим и и з ­ м енениями, а в и х последстви и с изм ен ен и ям и сук ц есси и расти тель н ы х сооб­ щ еств.