GEOL. CROAT. 46/l 7 1 - 90 14 Figs. I I ZAGREB 1993 I 
UDC 551.312:551.79(497.13) Original Sdenl ific Paper 

Alternating Lacustrine-Marsh Sedimentation and Subaerial Exposure Phases 
During Quaternary: Precko, Zagreb, C,·oatia 

Josipa VELIe and Goran DURN 

Key words: Pl eistocene, Holocene, Lirnnic, Paludal 
and fluviatil e depos it s. Loessoid , Palaeoclimate, 
Paiaeosol, Conditional marker hori zon Q', Precko, 
Zagreb 

Abstract 
Wo,;sl of Zagreb, v. ithi n an area of (1 ha , four units to!illling 60 III 

thil'knc:.s have heen recogniLcti 0 11 the ba:;is o f ('ore ana lysis, go.:ologt­
call1lappin g, gCllphysic'llmcasur.:mcn ls in explorat ion well s and lah­
or.llOI)' an:llyscs. '11l.! deepest situated unit (L~ni l I) aco.:u nwlatcu Jur­
ing the I.ower Plci!'. toccnc. It is inte rpreted to have fonned by accu­
Tllula!i\)11 of I ~)ess mixed wjlh local mat eria ls (loessoiJ ). Unit IT is 
cons id e rcil II) he Midd!.: Pleistoce ne in age. While in its luwer and 
nliddlc pan fluvlati\c · lacustrine sed im en ls are recognil.cd, in thc 
ll!l!lCr lXll1 aCI)! i;l n Illa! eria l cOll!ribu!eu to the t'ompo~i t ion of the sedi ­
ments . This Un!! is ove rlain by Unit III whidl is consi,kred to b¢ 
Upp,.:r Pleistocene in age. 'nw composition of thc ullil is JOlllin:H cl ! 
uy 11l,lIaial of loess origlll, and is interprcteJ to havc fonncd in a 
marshy cnvironlll cnt. Th.:: young.::st unit (U nit IV) is composed of 
Iloln..:cnc fluviatilc l'cdilllo.:n ts. "I"ho.: llpper parts of Un its I, II and [[I 
display palaco~ol fealures inJicating Ihal wcre subjccted 10 Ihe a";lion 

o f soil fOlllllng prOt.:esses Junng phases nf suixlerial exposu re . ThcS\: 
occuro.:u as a rcsull of lake/mar .. h in fi lling whidl happened Ju ring the 
CI)ld and .If)' gbdals :md prohab!y lasted dunng the olde r l~riooJs of 
int c rgt.J.ciab. Re:-'Ulllption of shal low and quiet WOller cllvironmen ts 
llunng the younger pe riods of intcrg lacials is (."ongnums wil h the 
illcrca!'>Cd influCllce of humiJ ity. T he fo nnalion of bot h, SI"lo.:clfi.: S<!lli­
menlary environments and phases o f suhaeri al cxposurc was also 
innuenco.:d by differently di sp1:Jycd neotectonic ;lClivity which was 
only pailly cOnll"lo.:nsated for by sedimentati on amI delludalion respec ­
tIvely . 

I. INTRODUCTION 

Drill ing and geophysical measurements undertaken 
within an area of 6 ha south of Precko (Western Zagreb, 
Fig. 1) have allowed the study of the lithological COIll ­
posi tion, pal eoenvironmental reconstruction and srrati ­

graphic relationships of the deposits. in part, this paper 
represents an ex pansion of investigar ions calTied out by 
VELIC & SAFTIC ( 1991) 10 kilometer westwardS, 
along the left bank of the Sava ri ver. in the vicinit y of 
its confluence with the Krapina ri ver. They defined the 
condit ions and processes of formation of the Middle 
Pl eistocene Illiviatile- laclistrine Hnd Holocene tluviatile 
deposilS. 

Kljucilc rIJCCI: Pleistocen, holocen, lilllnicke, palu­
dalne i tluvijalne taloiine, lesoid, paieoklima, pale­
otlo, lIvjetni reper Q', Precko. Zagreb 

Sazctak 
Zapadno od Zagreha, na povrsill l od 6 ha na ~1..;rlOvi rew li :lfa 

bll~e llja, geofizickih mje renja II busotinama , tercnskc dctenllinacije i 
laboratorijskih analiza, r,lLlucene Sll celiri jcdinke do tl ubine 00 60 
Ill. NaJduhlja, jedilllca I nasla!a jc tijekolll Jonjcg pleisloccna ll akup l ~ 

janjem 1csa LIZ mijesanje s Inkalnilll lllatcrijalo])l (lesoi J). lcdinica II 
jc srednjop1cislocenska. U donjc1l1 i srcdnjclll Sl1 dije lu z:l stuplj cni 
rijccllo ·jczerski, a u gnrnjc T)} sve vise i eol..;ki scd im enti . Slijedi 
jCl!illica Ill , gomjnp1cislocenska, uominantno ! c~ l1()g podrijella, aku~ 

Illulirana II Ill~)cvari. NaJllllada j..: jedini'::l IV , izgr,ldena OIl holnccn~ 
skog rijc'::nng nanos;l. Vr.~lIi dijclovij eJi nic;l!, II i III i1llaju i'.l1aeajkc 
paleotala buduci su bili il.lo1-cni peJogc llcz i. Kopncn c fal.C Sli rCI'.ultat 
za punjav:lnja jei'.c ra/l11ocvara tijc kolll hladni h i su hih gladjala, a tra­
ja1c su t stano\'ito vrijelllc k roz s larija rat-doll!j a inlcrgla..:ija!a . 
Suk ladno svc vccem Iltjccaju hUlllidi tel;J, lJ mladilll r;l'ldooljilll;l inter· 
glacija la ounavljane su plilke, ;llimc "oelenc sretline. Na up naslaga i 
pojavlL kopncnih fa'l';l uljeclla jc i ralli c ito laa1-CII<l lokaln:l llcotck­
\on ... ka ;lklivllost koja je sa1110 Ilje lom i..::c kOlll l"lo.:ll/j rana seJil\l Cll t aci~ 

jonl, oonosno dcnudac ijl)m. 

Many reconstructions. especia ll y for Ih e Late 
Quatern;uy, based on continentaJ hydrolysis. sea water 
and general temperature are availab le for marine 
records (e.g. ROTSCHY et aI. , 1972) . Compared to Ihe 
continent.al environments, slIch as cave fillings, tluvio­
glacial. or tluvio~ lilllnic depOSits, they indicate a clear 
sequence of depositional history. Alt hough mainl y of 
local significcUlce, results based on the in vestigation of 
specific continental environments, accompan ied with 
observed lateral and vertical changes can undoubtedly 
increase a level of knowledge of events thm have taken 
place during Quaternary. 

The area of investigation represents a low land, aver­
aging 120 rn above sea-level. covered by meadows and 
mabie land. Seven exploration well s were drilled: fom 

r .. ..::u lt y o f ~ining, Geology and Pe troleu1ll Enginee ring, Pi~rOllijcva 6, 41000 Zagreb, Croatia. 



72 

Fi g. J Localioll map. 
S]' I Polo:i.ajna ":l11 a . 

o , 50 laO km 
.....I I 

along the left bank and three along the right bank of the 

Sa va ri ver (Fig. 2). A total of 390 m of ex ploration core 
IllClleri:l1 was extrac ted and anal ysed. More th~Hl 30 
sa mples were collected fo r laboratory inves ti gations. 
Natural and induced riluioactivity measurements were 

al so undertaken. 
Geophysical mC:1surcmcnts conducted in the study 

area indic:uc the ex istence o f four di stinctive units 
which cOITcspond wilh the litholog ies ascertained from 
field ;lJld drill core Illapping. Zones with features indi­
cating the influence of soil forming processes can be 
defined. It has 10 be stressed that these zones arc closely 
related to the boundaries which were observed between 
the units. The related lIliits are characteri zed by specific 

granulometric composi tion. pebble litho logies, relative 
frequenc ies o f OCC UITence of se lected heavy minerals 
anel, p;utl y, bulk ,mineral composition of sands, ~ ilts and 

silly-clays. The stuely recognises specific characteris tics 

as the consequence o f seciimcnt;llion in different envi ­
ronments and paleoc limati c condition s and , postsedi ­
mentary processes during the phases of subaerial expo­

sure. 

2. REVIEW OF RESULTS AC IlIEVED fiY 

PREVIOUS STUDIES 

Already at the beg inning of cen tury the idea was 
stated that yell ow (lnd grey coloured diluv iulll deposits 
of the Savel plain represented sed iments of marsh or 
lake env ironments th at had exi sted si nce the U pper 

Pliocene (GORJANOVIC~KRAMBERGER . 1908). 
A fter 1908, investi gations of the Quatern;uy sediments, 
loc<lted in the Zagreb environs, proceeded in two direc­
tions. H ydrogeo log ical in ves ti gati ons (M ILETIC & 
BORCIC. 1967; NOV INSKA el ill .• 1967; BORCIC el 

GCI)If)gi~ Cro;llic:l Mi/l 

Fig. 2 Lu.:aliotllllapnfw..:lls . ugl! lul: l =wl!ll. 
St.2 Kalla raspI)f";I!a hU ;lIlill :l . i .cg..;nl ia : J=o/.l1aka I .a bu;:'olinll . 

aI. , 1968; CAKA RU N e l a l. . 1987) focu sed o n gravel 

hori zons while others concentrated on petrological and 
stratigr:lphical problems. 

It has been es tablished that in the vicinity of Precko, 
the s:lJldy-silty-clayey. meter th ick superficial deposit is 
underlain by several formations; all approximatel y 10 rn 
thick , predom inantl y coa rse-grained gra ve l overlies a 
brown. gra ve ll y-clay and 1IIH..Icr ly ing. greasy, grcy ish­
blue clay, sim ilar to the Young Pli oce ne and the Z:lgreu 
Ple is loce ne le rrace de pos il.'. CRN KOVI C & BUSI C 
(1970) pointed out the ckar dependence of tile Illincr­
al ogicH I-pclrographical composition of Ihe Sav:, ri ver 
del.)Qs it ~ on the litholog ic.1I composition of the drain:lge 
area. Between Zapre!;ic and Rak itje, cobbles o f mainly 

dolomite-limestone composition are found. w hile due 
ea ~ [ , w ith th e rt ppea rance o f greenschi sl s from MI. 
M edvednica. the composition of cobbles changes, w ith 

qu:ut z being more frequent. Us ing factor analy sis. 
RAFFAELLI & MUTI C ( 1982) separalecl heavy miner­

ai assemblages and concluded, that the material , salll ­
pled in the U pper Plioce lle - Ple j ~ t ocene deposits, 15 kill 
due southeast of Precko, predominanrly origin,lIcd from 
the metamorphic rocks of. mo~t l ikely , M I. Moslavacka 
Gora ~nd is partly of :leolian orig in . Sedi mentation of 
the material took place in a quiter environment. 

The Ill ost detail ed study on th e Quaternary sedi ­
m ent s situat ed in th e Z~g re b env irons is th .. n o f 
SIMUN IC & BASCH ( 1975). In 120 m ex pl oration 

core material, they recognized four horizons of maJ"shy­
loess and three hori zons of flu viatile deposi ts which me 
considered to be from the Riss to the II I \Vlinn stad ial 
in age. S IKIC e l al. ( 1979) a nd SIKIC & BASCH 
(1975) consider that detai led division of the Plei stocene 
depos its of the western p;u·t of the Zagreb environs is 

imposs ibl e, <lpart from divi sion into genet ic ty pes, 
which are pondy-loess, cont inental loess w ithout car -



Vclie & Dum: Allc m31ing L3CUSlrinc-M:H~h ... 

bonates, alluvial deposit of the third Sava ri ver telTl\ce 
and cave~ fillings . During the Plei stocene, pondy-loess 
was deposited in lake-remnants and/or ponds wi th a 
periodica l flu vial inflow. 

The QUil ternary deposits investigated in Prev laka, 
<lIang the Savel ri ver , located about 45 kill due west of 
Precko. :lre :l lsO documen ted in detail. A lthough located 
distant to the position of the present study, thi s area 
lI1uSt be discussed. While HERNITZ et nl .. ( 198 1) 
emphasized th:lI the Holocene and Upper Pl eistocene 
deposits together, arc lcss than 20 III thick, SIMUNIC et 
"I. (1988) pointed out that 73 111 of Upper Pleistocene 
deposits are overlain by 2 to 3 rn thick Holocene sedi­
ments. Results of the in vesti g;:lIioJls perform ed under­
line the difficulties and dilemmas concerning the 
chronostratigraphic subdiv isions. 

3. ~IETIiOLlOI.OGY 

On the basis of descriptions performed and intervals 
observed. a qui te limited number of representative sam ~ 

pies were taken and subjected to different types of 
ana lysis. Grilll ul omelric analyses were obt"ined by wet 
siev ing and sedimentation balance. Petrogr<'lphic deter­
minations of sandy ~grave ls and gravelly~s;lnds ( 17 sam­
ples) were achieved by establi shing relati ve frequencies 

S 569 700 5 569 800 5559900 5570000 

73 

of occulTence of cl<-'l st lithologies in the fraction> 4 
Hun . In addition , thin-sect ion analyses of selected peb­
bles were pelformed. The 7 1 to 125 >,111 fraction of the 

selected silty-&1n<ls and silts (15 samples) was quantita­
ti vely se parated into heavy and light f racti ons using 
iJromoform. In order to determine the relative frequen­
cies of OCCUITence of the mineral s, counts of the grains 
were made microscopically. XRD-da ta of se lec ted 
sands. silts and silt y-clays (13 s,"nples) were obtained 
using n Phillips X~ray diffractometer unit. w ith ell K a 
radiation generated <'It 34 kY :In<l 18 mA. 
Scmiqu<'Intit<'ltive estim:-ltion of mineral content was per­
fOllned as wel l, Micropal;leontological investigations of 
se lected Silty-sa nds were also unden"ken. 

During explor<llion. wel ls were measured for natur:c, l 
Clnd induced radioacti vit y. In :ldditi on neutron log mea­
surements were performed. \Vhile an excellent verti ca l 
resolution has been achieved with the natural rad ioac­
ti vit y measurement s. onl y the neutron curve confirmed 
the existence of some horizons on a I imited scale, wi th 
increased moi stness or ground -wa ter saturated hori ­
zons. 

Allhough the limited number of s:lIllples and analy­
ses made interpret:lIion spor:1di c:lll y difficult , it has 
been compensated for by an interd isc iplinary synthesis 
of the results obt<'lined. 

4. LITHOLOGICAL DESCRIPTION OF UNITS 

4. 1. INTRODUCTION 

5 Discrimination of units is based on all the field and 

20 

22 
24 BP-S 

J 

PP-2 

~ 
0,1 

Legend : 1 ~ L egf!nda : 

t 22 

BP-4 ~ 
o 

t km 
I 

20 

Fig. 3 Isopal: il map uf Unit I!. Legend: l = i ~opach. 

071 0 900 Iaborarory delta. n the basis of core determ inations, 

5 
071 
'00 

5 
071 
700 

5 
0 71 
'00 

b 
500 

results of applied laboratory analyses and average nat­
ural radioact i vity, four units can be recognized. 

A 13 to 25 meter thi ck interv,"ll of U nit I was 
encountered in all wells. but the base of the unit was 
never determined . During the field work, certa.in char­
acteristics were noticed which clearly distinguish this 
ullit from the overlying sediments. These are a grade of 
diagenesis, uniform granulometric co mpos ition and 
colour. The unit is composed of yellowish-orange, yel­
low ish-red and yellow ish-brown. se llli ~ lilhifi ed , com­
pact clayey-silts and silt y -clays. G rey coloured or 
brown ~ mottled. meter thi ck interbeds are present , 
together w ith a few decimeter thick lenses of s:CUld , and 
a minor amount of gravels. 

Unit II i s of relati ve l y un iform compo sition. 

SJ. 3 Karta d..:h ljinc II jcdinice. Legenda: l =li llijejcdnakih dchljina . 

Ranging in thickness from 10.35 to 24.3 III (Figs. 3, 6 
and 14). the lower part of the unit is predominantl y 
composed of grey-coloured sands. Upw(lrds. the con­
tent of silt and clay sized material becomes significant. 
Unit 1 is directly overlain by 0.5 to 2.5 III thick gravel­
Iy ~sands, containing tip to 33% gravels. Their base is 
sharp , and they pass upwards into sands with varying 
proportions of silt. In the middle port of Un it II , a 1.5 to 
3 111 thi Ck. sellli ~ lithi fied layer of normally graded grav­
ell y-sand is present. which grades upward into fine 



74 

sand. The upper part of the unit is dominated by grey­
coloured or, less often, red to yellowish-brown mottled 
silt and clay sized material with weathered carbonate 
concretions. 

Unit III is heterogeneous and varies in thickness 
between wells, as shown on Fig. 4. The minimum 
thickness of the unit was observed in exploration well 
BP-5 (6.5 m), while the maximum thickness was found 
in BP-3 (13.2 m). The oldest (and basal) member, a 
poorly sorted mixture of gravel, sand and silt, 
(-33:33:33%) was observeci only in two wells. 
Elsewhere, the base of the unit is represented by clays 
and clayey-silts. In wells BP-2, BP-3, BP-4 and PP-l, 
these sedilnents are overlain by sands which become 
progressively more silty. In distinction from those pre­
viously described, in wells BP- I, BP-5 and PP-2 the 
lower pm! is silt dominated, while younger intervals are 
more sandy. The colour of the unit is not uniform. 
While the sands are predominantly grey-coloured, the 
silts and clays are often mottled yellow and brown. The 
uppermost, 10 to 70 centimetres of the unit, as 
observed in 6 wells , is rusty to yellowish-brown in 
colour, and the boundmy with the overlying Unil IV is 
characterized by the abrupt apretlrance of gravels and 
sands (Figs. 6 anciI4). 

The youngest unit (Unit IV) varies in thickness 
from 6.6 to 7.7 m (Fig. 5) and is of a simple lithological 

5 '569 700 5 569 800 5 569900 

B;3-3 \ 
1ZJ 

11 __ -

10---

BP-1 

" 

PP-I 
o 

~ ~/0 h 

J~p-z \, 
o 05 

Legtnd : 
Legf'nda : 1~ 

BP-, 
o 

9 

lkm 

Fig. 4 Isopach l11ap of Unit III. Legend : I=isopach. 

5570000 

5 
071 
900 

5 
071 
'00 

5 
071 
700 

5 
071 
.00 

SI . 4 Kart a tkhljine jeJinicc III . Lcgcnda: l=linijc jcdnakih debljina 

Geologia Croatica -1(,/1 

composition. In wells PP-l, BP-3 and BP-5 carbonate 
gravels, comprising well rounded cobbles of up to 7 
cm in diameter were recognized, accompanied by pale, 
yellowish-grey sands. E lsewhere gravels and sands are 
overlain by a greyish-brown, fine-grained silty-sand, 
less than I m thick, with rare cobbles of carbonate 
composition. The brownish colour is a consequence of 
the presence of carbonized plant remnants. The oIigin 
of a ciesn-oyed peat is possibly related to the adjacent 
subrecent marshy areas which were incorporated into a 
fluviatile-type environment. 

The general lithological characteristics of the units 
described above cOlTespond to, and are retlected in the 
geophysical signatures of the sediments (Figs. 6 and 7). 
However, trnces observed from different well- logs can 
indicate Illutually opposing tfends for zones of simil.;-tr 
age e.g. Unit III, wells BP-5 and BP-2 (Fig. 6). In addi ­
tion, the pattern of the gamma log can, in some 
instances, be directly related to the litholog icaL compo­
sition. For example, these traces in Unit III (see well 
BP-5, Fig . 6) form a funnel -like pattern in the lower 
part of the unit, diverging into a bell-shaped pattern in 
the upper parI. These patterns cOlTesponcls to increasing 
gravel content ill the lower pmt of Unit Ill, and the 
higher sand, silt and clay content of the upper pm'! of 
the unit. 

As observed in Figs. 6 and 7 the boundaries 

5569 700 

BP-5 
a 

BP-J 
a 

'5 569600 

pp -z 
a 

5 569900 

PP-I 
o 

BP-I 
o 

5570000 

S 
071 
900 

, 
07 1 
000 

~--~5 

BP-' 
a 

5 
071 
700 

5 
071 
'00 

L ____ ~~O:.::::::~::O:,5::::::::::~lk_m ______ ~~71 500 

legend; 
Legenda : 1~ 
Fig. 5 Isopach map of Unit IV. Legenu: l=isopach. 
SI.5 Karta debljine jedinkc IV. Lcgcnda: I =linije jCllnakih dcbljina . 



Velie & Dum: Ahematin!!; Lacustrinc-M:lrsh. 

1m ) 

'25 

120 

11 5 

110 

105 

100 

95 

90 

B5 

so 

75 

70 

BP-5 BP-2 

11' 

neutron log 

gamma - gamma log 

Fig. 6 Well- logs lToss-currclation BP-S - BP-2 - BP-3 - PP- L 
SJ. 6 Shclll atski bnclacijski profiJ Br-S - BP-2 - OP-3 - PP- 1. 

1m) 

'25 

'20 

115 

11 0 

'OS 

100 

55 

90 

65 

75 

70 

" 

PP-2 

,----, 

gamma.! 
log 

: 59° i----

neutron log 

gamma-gamma log 

BP-4 

Fig. 7 Well -logs cross-correlation PP-2 - BP-4 - BP- l . 
SI. 7 She[llatski korelacijski profil PP-2 - BP-4 - BP-l . 

BP-3 PP-1 

60' 

BP-1 

10' 

Q' 

'" Z 

'" IV g .... 
o 
::t 

III '" 

z 

u 
II 0 

.... 

'" IV ffi 
u 
o .... 
o 
::t 

III 

z 

II u 

o 

I-

UI 

.... 

75 



76 

5569700 5 569 sao 5 569900 5570 000 

86 

85 B~1 
84~ O 

83 
82 

81 8P-S 

800) 

Ll'g~n d: 
Legenda : 

pp - 2 
o 

0,5 

80 

Fig. 8 (\)llh)Urmap - base of Un it II. Lcg~· n.l: I:i!'ohyp!;e. 

5 
071 
900 

5 
071 
800 

5 
071 
700 

5 
07 1 
600 

Sl. 8 K:u1a 1'lI.1lii nlike pll)l\.; jedinice II. l...::gcnda: I =1inije jetlnal ih 
ap!'olurllih v isin:L 

between un its are not p~uallcl. reflecting lateral th ick­

ness variation of the units. This is al so c learl y seen in 

contour maps of the bound;u'ies (Figs . 8, 9 and 10). The 
steepness of the slope of the boundaries (reflected by 
tile spaci ng of lhe contours) decreases for progress ive ly 
younger bOlln d~u ' i es (compare Figs. 8, 9 and 10). This is 

the consequence of a nUllloer of f<lctors, including sedi ­
mentary environment s, sedimentation and denudati on 

processes. anel tectonic processes, anel is disc Ll ssed fur­
ther below. 

4.2. DET AILED DESCRIPTION OF UNITS IN 
DR ILL CORES BP- I AND BP-4 

A fter the detai led anal ys is of drill cores, wells BP~ I 
~nd BP ~ 4, charac ter i zed the mos t obv ious lateral 
changes between contemporary units and were chosen 
for compari son. While drill core BP-2 di splayed quite a 
high degree of similarity on granulollletric and mineral 
ch:mlcteri stics wi th dri ll core BP-I, drill core PP-2 di s­
played the same with drill core BP-4. These facts were 
used in order to supplelnent and exp<lnel the data. 

Vllit I 
BP- l drill core was tennin;lIed in Unit I at a depth 

of 39.2 111 recording a thickness of 15.8 111 , but the base 

-

-

5569 700 5 569 900 

~P-~\ 99~ 

100 

101 ____ _____ 

o 

BP-2 
o 

Gcolngi:1 Cro:lli<;a 4(,/1 

S Sf>99oo 

PP-t 
o 

------\\)'1-
BP-t 

BP - 4 
o 

o 

I km 

os 570000 

5 
07 1 
'00 

5 
071 
'00 

5 
07 1 
700 

5 
07 1 
500 

5 
071 

~ ____ L_~::::::~::::::::==~::~ ______ ~500 
Legend: 
Leg~nda ~ 

Fig.9 Contour 111.l p - has..: of Unit III. Legend : l = i ~(lhypsc. 

SI. 9 Ka rl a pod in .. ke plohc j,;d inc..: III. Lege nda: 1=li nijc j..:dnaki h 
apsutlltn ih \·i .. ina 

of the unit was not determined (Fig. 13). In ascending 
order the unit consists of: 

55.0 - 53.9 rn , predominant ly yellowish-brown mot­
tled, grey-coloured cl::lyey-silt with sporad ic quartzite 
and s(uldstone granu les. 

53.9 - 50.0 m, ye llow i, h-brown cb y anel ye ll owish­
brown mottl ed silty-clay with sporadic pebbl es. 

50,0 - 49 .6 ill , predominantly yellowish-brown mot­
tled grey clayey-silt. 

49,6 - 47.4 Ill, yellowi sh-red silt y-clay wilh sporadic 
gran ules in the lo wer part of the leve l (lnd ab lJndant 
quart zite and sand stone pebbles ill the upper parr, 

47.4 - 45.3 fl 1. ye llow ish-red , silt y-clay to clayey-s ilt 
with sporadic quartzite and sandslOne pebbles, A thin 
interbed in the lower part of the leve l represents green­
ish-grey to brown, poorly sorted gra velly (0 silt y clay. 
The fraction >4 mill contains Inainly quartzite (68 70) 
~lnd sandstone pebbles (26 ('/0). Ex trusive rocks , tuffs 
and schists contribute a few per celli each, The Heavy 
mineral fraction contain s opaqu es (62%), epidote 
(23%), zois ite (7%) , tourmaline (3%) , eli"hene (2%), 

zircon, garnet and apatite ( 1%). 
45 .3 - 39.2 m, yellowish-recl mottled silt y-clay with 

sporadic limonitic sflndstone pebbles . The Illoo les men­
tioned are mostl y assoc iated wit h the upper part of the 
leve l. XRD -anal ys is showed that the ye ll ow ish-red 



Vcli0 &: Dllm: AlterrntiTlg [.:lc!lstrim'. :"b r~h ... 

5 569 700 

BP-5 
o 

BP-3 
o 

5 569 900 

PP -2 
:::: 0 -o 

Ltgtnd : 
Legenda : 

l~ 
L1Jd 

PP-l 
o 

BP-2 
o 

BP-' 
o 

5570000 

5 
071 
900 

5 
071 
eoo 

5 
071 
700 

5 
071 
600 

Fig. [0 Contour llIap - uase of Un it IV . Legcnd : 1==isohypsc. 
Sl. 10 K;lJ1a poO:\ in ske p1nhc jcdillice IV. LcgcIl<1a: I=Jinijc j..;,1T1<lkih 

apsollitnih visilla . 

mottled si lt y-clay cons ists of qlJartz (38%), mic~ceolJ s 

minerals (23%), K-feldsp;u· (2%), ch lorite, unidentified 
mixed-layer clay mineral , kaolinite and goethite, 

In drill core BP-4 Unit 1 is 22 III in thickness, but 
the base of the unit v·,Ias not determined (Fig . 14) . It 
consists of: 

55.0 - 54.2 m, predominantly yell ow ish-brown mot­
tl ed. dark grey sil t with sporadic quanzite pebbles. 

54.2 - 53 .8 Ill , dark grey-greenish silt to fine grained 
s:l nd. 

53.8 - 53.3 Ill , dark grey co loured, sandy matri x sup­
ported breccia-conglomerate. 

53 .3 -52.8 Ill , fine-grained yellowish-brown mottled 
sand, fining upwards to grey silt. 

52.8 - 43 .0 Ill, ye ll owish-brown clayey silt with grey 

mottles 
43.0 - 40,0 m, yellowish-red silly-clay to clayey-silt 

wilh sporadic grey mott les. 
40.0 - 33.0 Ill , grey silty-c lay to clayey-silt with yel­

lowish-red mottles. A sample taken from the upper pmt 
of the level conta.ins qu:u"tZ (20%), micaceolls minerals 
(30%), dolomite (15%) , ca lc ite. chlorite, smect it e, 
mixed layer clay mineral and kaolinite. 

77 

Un it II 
In drill core BP I Unit IT is 23 .8 m thick, Contact 

with the underlying Unit 1 is sharp and is characterized 
by an abrupt change in granulometric composition and 
colour. 

39.2 - 32.8 m, grey gravelly-sand and silty-sand, grad­
ing upwards to sandy-silt and sandy-c layey-silt. The 
heavy mineral fraction of th e si lt y-sa nd contains 
opaques (78%), gamet (7%), epidote (5%), zircon (3%), 
titanite, chlorite, di sthene, apatite, zoisite and tounna­
line (\ %). A sample of the sandy-clayey-silt consists of 
quart z (28%), micaceous mineral s (20%), dolomite 
(15 %), plagioclase (8%), calcite (7%). chlorite, smec­
tite, mixed-layer clay mineral , kaolinite and, poss ibly 
siderite!. 

32.8 - 27.0 m, grey sandy-silt s overlain by alternating 
dm sized grave lly-sand layers and cm -elm sized layers 
containing silty-sands. The gnwelly-sand contains peb­
bles of quartzite (53%), sandstone ( 17%), chert (14%), 
limestone (5%) , dolomite (4%) and cong lomerate-brec­
cia (3%). A lso observed extrusive rocks, tuffs, and acid 
intrusive rocks contribute a few per cent together. 

27.0 - 21. 5 tn, grey si lty-sand. Consists of qu~u·tz 
(30%), dolomite (28%), micaceolls minerals (j2l'/c), cal­
cit e (8%), plagioclase (5%), K-feldspar and chlorite. 
Heavy mineral fr(]cti on conta ins opaques (62%), garnet 
( 12%), epidote (9%), zoisite (6%), chlorite (5%), zir­
con, amphibole, disthene, apatite and tit~nite (1 %) . 

2 1. 5 - 19.9 Ill , ye ll ow ish-grey sa ndy-s ilt with thin 
interbeds of silty-clay. One of the interbeds contains 
qlJartz (22%-), micaceous minerals (25%), doJolllite 
(20%), calcite (5%), K-fe ldspar (3%) . chlorite, smectite 
and mixed-layer clay mineral. 

19.9 - 19.0 111 . greenish-g rey sandy-clayey si lt w ith 
carbonate concretions. 

19.0 - 18.0 m, predominantl y grey clayey-s il t with 
yellowish-brown mottles, carbonate concreti ons nnd 
rem~tin s of Rhisoconcretions. 

18.0 - 15.4 111. ye ll owish-llrow ll 1I10ttied clayey-silt 
with cnrbonnte concret ions. 

Tn drill core BP-4, U nit 11 is 16.6 III thick. Contact 
with the underlying unit is not sharp but distinguishes 
itself with a marked change in colour. 

33.0 - 31.0 m, grey sandy-si lt 
31.0 - 28 .0 m, li ght grey sandy-si lt wi th rare pyrite 

crysta ls. T his passes upwards to grave ll y-sa ndy-si lt 
with th in greeni sh -grey interbeds of si lt. A silt sampl e 
contained quartz (16%), micaceous mineral s (10%), 
dolomite (30%), calcite (15 %), plagioclase (3%), chl o­
rite. mixed-layer clay mineral and, possibly siderite. 

28.0 - 26.4 rn, grey silty-sanely grave l. The fraction> 
4 mm cO/llains pebbles of sandstone (36%), quartzite 
(49%) alld chert ( 12%). Pebbles o f ex tru sive rocks, 
tuffs. acid intrusive rocks :md schi sts, contribute togeth­
er a few per cent. 

26.4 - 22.9 rn , grey silty-sand. The heavy mineral 

t According tl) XRD uata, ab~crvcd u ni dent ifieu carbonate minerals, noticeu in some sam pl es can Ix l"<:t"crcd la sidctito: in whi ch iron is part ty 
r..::placed with calciuTll and tllanganese (Prof. D.slovenec, personal COlllllllltlicatian). In the further t~xt, tenn possible sid~rite will he used. 



78 

fraction is composed of opaques (79%), epidote (7%), 
zoisi te (5%), garnet (4%), zircon (3%), tourmaline (I %) 
as we ll as apatite, chlorite and disthene (contributing 
less than a per cent each). The mineralogical composi­
tion of the upper pmt includes qUaJ1Z (40%), micaceous 
minerals (8%), dolomite (28%), calcite (6%), plagio­
c l'tse (5%), K-feldspm (3%) 'Uld chlorite. 

22.9 - 19.7 m, as the underlying material but with an 
increased silt content and thin sandy-si lt interbed. 

19.7 - 16.4 m, greenisll -grey sandy-c layey silt with 
sporadic pebbles and irregu lmly distributed cmbonate 
concretions. 

Unit III 
In drill core BP- I, Un it III is 7.7 III in thickness. The 

bound,m"y with the underlying unit is emphasized with a 
marked change in colour. 

15.4 - 14.7 m, greenish-grey sandy-clayey-silt. 
14.7 - 12.7 111, greenish-grey clayey-silt. The mineral 

composit ion includes quartz (38%), micaceous mineraJs 
(25%), plagioclase, chlorite, smectite, mixed-layer clay 
minerals rmd kaolinite. 

12.7 - 11.2 rn, greenish-grey sandy-clayey s ilt with 
sporadic plant fragments. 

11.2 - 9.5 Ill, grey sandy-silt with ostracodes and 
rema ins of LifhoglyphllS sit uated near the top of the 

sequence. 
9.9 - 8.7 m, yellowish-grey silty-sand. 
8.7 - 8.4 m, grey silty-sand. 
8.4 - 7.8 tn, silty-sand, yellowish-brown mottled in 

the upper part, yellowish-brown in the lower pmt. The 
heavy mineral fraction contains opaques (43%), gamet 
(25%), epidote (9%), zoisite (5%), chlorite (5%), 
apatite (4%), zircon (3%), tourmaline (1%) as well as 
disthene, rutile, titanite, staurolite and sillimanite. 

In drill core BP-4, a 9.6 m thick Unit III was 
encountered. The boundary with the underlying unit is 
sharp and marked by an abrupt change in granuJometric 

composition and a s light change in colour. 
16.4 - 15.4 tn, grey, ungraded, sand dominated mix­

ture of gravel, sand , silt and c lay with a pyritized frag­

ment of wood. 
15.4 - 15.0 tn, grey silty-gravelly-s:md with pebbles 

of dolomite (3%), sandstone (25%), qumtzite (45%), 
ext rusive rocks and tuffs (6%), chert (13%), and some 
acid intrusive rocks ;md schists. 

15.0 - 10.4 m, grey si lty-sand with a brown coloured 
interbed containing plant remnants and fragments of 

wood. 
IDA - 7.5 m , grey silty-sand. 
7.5 - 7.1 m, greenish-grey c layey-silt with irregu lmly 

distributed carbonate concretions. 
7.1 - 6.8 m, silty-sand with pebbles in the upper part. 

Unit IV 
Unit IV, co mposed of sandy-grave ls, ranging in 

thickness from 6 .6 to 7.7 m , sh,"pl y overlies Unit lIT. 
Diso'ibuted over the whole study area, sandy-gravels of 
grey, ye ll owish-grey and greyish-brown colour are 
composed of vmiety of rounded and subrounded peb-

bles set in a s ilt y-sand y matrix. Pebb le lithOlog ies 
include limeston es (49 - 55%), dolomites (5 - 2 1 %), 
sandstones (II - 23%), quart zi tes (8 - 13%), chells (2-
8%) , extru s ive rocks rlild tuffs (up to 5%), and con­
glomerates, breccias, acid intru s ive rocks and schi sts 
(contributing a few per cent each). 

5, RESULTS 

5.1. GRANULOMETRIC ANALYSES 

Unit I is laterally uniform and composed of s ilty­
clays and clayey-silts, with randomly distributed gran­
ules and pebbles. In the lower and middle parts of the 
un it , few sandy and gravelly-sandy layers were 
observed. Unfortunately, only a small number of sam­
ples were anrllyzed, so, the description of Unit 1 is 
b::L<.;ed ma.inly on field observations. 

The results of particle size detennin;ltions of Units 
1I , III and IV, in drill cores BP- l and BP-4 are shown 
on Figs. 13 and 14. Unit II is laterally homogenous and 
characterized by the presence of one or two gravelly­
sand seq uences. In the upper part of the unit, abundant 
si lt size material, accompanied by an increasing clay 
content is observed. Unit III d isplays ',nore lateral vari­
ation. While drill core BP-4 is dominated by sand size 
material, in drill core BP-l, the lower and middle part 
is characterized by a high si lt content. Unit IV is later­
ally uniform and composed of sandy gravels. 

The predomin<lnt occurrence of silt size material, 
observed in certain intervals of Units I, II and III, raises 
the possibility of loess contribution to the sedimentary 
basin. For the determination of sedimentmy environ­
ments based o n particle-size distribution, the correla­
tion of the parameters med ian, coefficient of so rting 
and skew ness have proved convenient (KUKAL, 
1971). According to KUKAL (1971), the median (Mel) 
of loess is usually 0.06 - 0.02 mm, the coefficient of 
sorti ng as Phi Deviation is 1-3 and Phi Skewness is in 
most cases sl ightly pos iti ve. 1n his figures, the coeffi­
cient of sorting and skewness of the sediments ;ue COI11-

pared with their median. The statistical parameters of 
the silt samples are plolted in Fig.12. The diagram is 
modi fied after KUKAL (197 1) and Nll-lLEN & SOLY­
OM (1986). 

It is obVious that the loess influ ence can not be 
neglected. Sand, or c lay sized material can be attributed 
to the mixing with local materials or to pedogenic 
processes. According to PYE ( 1987), the term " Ioes­

said" can be ll sed to describe sediments composed of 
mixtures of deposited dust a nd other (local) sed iments 
(such as dune s.md, soi l, alluvial fill) . He also e mpha­
s ized that the term " loess-like deposits" can be used for 
sediments which possess many of the sed ime ntological 
properties of aeolian loess but w hic h have not been 
transported by the wind at any stage in the ir hi story 
(such as overbank s ilts and some colluvial deposits). 
Loess is frequently but very often a mi s-used term in 



Velie & Dum: Ahemating I~'custrille Marsh ... 

our literature. In tltis paper, for sediments having the 
propeJ1ies of loess (mainl y based on particle size analy­
ses and analogy with the l iterature), reworked loess and 
resedimented loess, the term loessoid sediment is used. 

5.2. PEBBLE LITHOLOGIES 

On th e basis of pebb le lithologies, two different 
types of gJ'Hvelly sediments can be recognized. Type I 
includes the si lty-grav elly sands of Unit III , gravell y­
sands (llld snndy-silty gravels of Unit II and gravelly­
sandy interbeds of Unit 1. They are of siliciclastic com­
position, comprised mainl y of quartzite and sandstone 
granules and pebbles set in H clayey-si lt to sandy 
ma tri x. While in Units II and III a few pebbles of lime­
stone and dolostone were found. no h'ace of carbonate 
pebbles was observed in Unit T. Type 2 deposits are 
represented by the sandy gravels of Unit IV, composed 
of rou nded and subrounded pebbles of predominantly 
carbonate composition (l imestones and dolostones) in a 
silt y-sandy matrix. 

The difference, emphas ized by the pebble litholo­
gies of the two types suggests that during their forma­
tion, di stinct source rocks were exposed to erosion and 
weathering. In addition, it can be stressed that , general­
ly. morc limestones and dolostones were eroded. acting 
as a progressively dominant source of pebbles for sed i­
ments of increasingly younger age. 

5.3. HEA VY AND LIGHT MINERAL 
COMPOSITION 

The heavy mineral assemblages me comparat ively 
simple. Samples selected from Units I , II and III con­
t.lin opaques. epidote, garnet. zoisi te. chlorite and zir­
con with smnll amounts of lOunnaline, apatite, amph i­
bole. di sthene, titanite, staurolite. biotite and silliman­
ite. A complete absence of pyroxenes, together with the 
sc:u sity of amphiboles may indicate that intensive abra­
sion and/or weathering have taken place, suggestin g 
that sediments are reworked. In addition, it is possibile 
that the source rocks did not contajn these minerals in 
any di stinctive percentage. 

Heavy mineral percentages in a particular unit are 
comparable for equivalent depths. A difference between 
the g:unct and epidote content among the units was 
observed. In order to compare the heavy mineral COIl1-
position alllong the units, data <'ire plotted in relation to 
epidote, zircon + tourmaline and garnet (Fig. II ). The 
fOflllcuion of three di stinct groups suggest, thai, possi ­
bly, different source areas and/or different transport fac­
tors were in volved. 

The light mineral fraction consi sts of variable por­
ti ons of quart z, feldspars (mainly albite, rarely K ­
feldspar), muscovite and calcite (as mineral and lime­
stone fragments) . It is necessary to stress that in the yel ­
lowish-red mottled silty-sands of Unit I , calcite was not 
found. 

79 

5.4. PALAEOSOLS 

"Palaeosols are soi Is that formed in the past on por­
tions of land surfaces that were sufficientl y stable for 
variable lengths of time to recei ve and retain imprints 
of soil forming factors'" (LECKI E et aI. , 1989). EINSE­
LE (199 1) stated that lake deposi ts are frequently asso­
ciated with fossil soils. According to KRAUS (1987), 
palaeosols in alluvial sed iments me powelful indicators 
of pal eoclimate, floodplain drainage and pauses of sedi ­
mentation. 

In order to establ ish whether certain intervals repre­
sent palaeosols. the following criteria were used: 

- different colour compared to the over lying and 
underlyi ng material. 

- presence of mottles, 
- presence of concretions and nodules, 
- evidence of progressive weathering of minerals. 
- presence of roots and organic matter frClgmeIlts. 
On the basis of the above criteria. at least three 

intervals are of possible pedogenic origin. These inter­
vals afe closely related to the observed unit boundaries. 
They indicClte that the upper pm"ts of the units were sub­
jected to soil forming processes. However, it should be 
noted that some diagenetic features (for instance, burial 
gleying) closely resemble that of soil s. 

, , 
Ion 

l'OIIl~ : 
L~g~nda : 

, " • • 

.' .' , 
n' o 
, 

tOO \ 

, , 
D 0 

ZIRCON .TOURMAIINE .... tOo\ 

,GJ,GJ,GJ·GJ,GJ 
·GJ 'GJ'~ {~}o0 

Fig. II Composition of selected heavy mincrats. 
L.t:gcnd : l=well fiP- 1; 2=wdJ I3P-2; 3=wcll fiP-3: 4=wc ll BP-4; 
S=wcll BP-S: 6=well PP-I; 7=wc ll pr-2: 8=Unit I; 9=Unit II: 
100Unit Ill . 

Sl. I I Sastav izabrani h teSkih Illinerala. 
Lcgcnda: I =hu sotina BP- l ; 2=busot ina OP-2: 3=bu ~otin DP-3; 
4 = busotina BP-4 ; S=busotin;l BP-S: 6 =bu sotina PP- l ; 
7=busotina PP-2; 8=jedinica I: 9=jcdin ica II ; IO=jcdi ni ca III. 



so 

5.5. GEOPII YSICAL WELL LOGS 

The gamma log trace represents a li thological indi ­
cator as well as a IIh:' llIod of performing corrcim ions. 
For the Q uate rna ry sed ime nts in North Croat ia , thi s 
method is suitable oo[h for cased alld uncased w~ lI s . II 
facilitates very good gene!":l l Lli scrimi nation of clayey­
silt s, sand s and grave ls rC:-' lk 'Cli veiy : the first are recog­
ni zed due 10 hi gh radi;lIion, d ue 10 the pre ~ell ce of 
potass ium frOlll fe llhpars nlld 11Ii caceolJ s m iner;l ! :; 
(grain s and c J a~ t s of ~Ollrce rocks), the second ;m,::: idell­

tified by mediul1I radi:lli on brought out hy the d:1 111p ing 

inlluence of nOll - radioactive quartz and the th ire! pro­
duce very l ow leve l s of rad iation from ca rbona tes 

which constitute the rn:ljority of pebbles in the youngest 

gravels. 
The gmnma log traces, obtained from seven expl o­

rati on well s, corroborate the ex istence of fou r IIllit s. 
Thi s C:1n be ck:1rl y see n in explorm ion well PP- l (Fig. 

6) . The olde~ t uJlit i ~ characteri zed wi th an average of 
30 Count s Per rvlinulc (c Ptvl) , Ullit II with an average 
of 15 CPM (exce pt in leve l s wi th hi gh s;ulli con ten!. 
h:lVing R CPM), Uilit 1][ wilh an average or :W CPM 
:lJ1d Unit IV , in geneLl!. \vith.5 CPM. 

T he :,hape of the neulron log reflects the qIJw1tit y of 

hydrogen in r ock s penetrated by explor at ion well . 
Therefore, the neul ron log is used for lll e'l.<; urin g Ill ois­

lure auO\'e Ille water tabl e ~\Ild 10lal porosit y tX',low the 

wat er I:lo le. The It ig he~ t results. as show n jn Count Per 
Second lln i t.\ (C PS), coincide w ilh w<u er- l>earill J;. gra v-

q 

4 
A 

, , , . , • J 
, • , • ~ , 12 • 

2. 1 2Z~ 1, . f.$rot~ 
J 'l6 , c.l 

Z 

·r~ .~' / t 

I , , , , , , , , • , • T I Mel . 

eb of Unit I V and mo ist. sandy inter val s of Un it II 
(FigS. 6 and 7). 

6. INTERPRETATI ON 

(, .1. SEDIMENTARY ENVIRONMENTS AND 
PHASES OF SUBA ERIAL EXPOS URE 

The evo luti o n of th e lIllit s inv es li g<ll cd \vas 

undoubtedly dependent upon g laci:ll/i lll erglacial cycles. 
Il is a comlllon belief that during tile glaci:ll pe r iods, a 
!;lrge :1Jllount of wind borne sill material ( loess) was 
bl ow n OLiI and accuillulated :-'OLllll o f til e glac iated 

regions, build ing extensi ve " eolian loess dcpo.'~ j t s . 

A s si lt size mate rial is prcuominan t in the cores 
invest igated, an auempt was Ilwdc to fi nd out '.d letl1cr 
tile .sediments of Uni t I were 1';111 1), composed or loess. 
Sli ght ly too hi gh coenic i e nt ~ ur sorting com pared to 
the ave rage values (Fig. 12). po:-.:-. ib ly ind icate the mi x­
ing of loess wit h local 1ll:lI eri :lI s ( Ioesso id ~ccl illl e ll t). 

Jlowcve r , ver y similar gr;l in !-'ize p:u :lIl1 cter :, were 
found for flood plain ba s iJl ~ (K U KAL, 197 1) \vhich 
during :1 wet and humid clim;lh:: incl ude I:lrge vegetaled 
marshes or sW<lmps Hnd permall ent lakes nnd pOilUS 
(ALLEN, 1971). A lth ou g h ge n e ti cal ly related to 
g laci:ll s, during: the more humid periods, 10l!ss is easil y 
eroded by running water and f1u vi;l l :lCli on ,HIll Ir;ln s~ 

ported as a reworked sediment to an <l cce~:-. i b l e sedi ­
mentary basin. During IrallspoJ L :IS we ll as (kpo" itioJl . 

B 

~I ~ -I 

, , 
" • 

!rl-2J 
6 

, 
0 

'~:~r>' 6 6 'l. 1 
, ~'j. 
"~q" , , • .,0, V 

t / 

, , , • , • T • Md + 

l a.t nd : ,[~,GJ ,G] {~{~·GJ ,G].[J] .[JJIOW L ~9 ~ n da : 

J:jg. t2 A. Ro.: l:l tion Ixtwco.:n nl ..:di ;ln and the coefficio.:nl I)f sOl1 i.lg . 

n . Rdallol1 b..: tw..:cn lll ..:ui :ltl and ske wness. O utlin cd alill dash..:d 1.\) IlCS inJicalc arc:Is with ' ypiC:ll1 oc..;s dcpo~j l s rati o~ . 

(llIoJlflt!J afl..: r KUKA\. . 1971 an d 1\'[111.(::;\ & SOLYOM, 198(,) 
Lcg..:nd: I=wcll OP- I ; 2=v. d J 81'-2; J=wdl DP-3; 4 =wcll DP-4 ; 5=\\..:11 fiP -5; (,=""...:\1 PP. I; 7=wdl 1'1'-2; ~=C ni l L 9= Unl' II : IO=L:ni l III. 

Sl . 12 A . Od llos i 7JllCUU mcdijallil i k rl<~ fjcij ..:nla sOr1 iranja. 
O. OJIlDS if'.Ill ..:du Ill cdijana i ko..:f icijcnlil asillleirijo.:. Uo kvin.:n\! i isc l1kan(: 7.Onr.: indiciraju J)()(lrulja llI111tar klljih so.: llala7.c ndllosi kn..: ficijc ­

niHa 1.,1 tipi ":nc nasI age k sa . 
(rn ndific irano prmn;\ KUKAI", 197 1 i :\lIILl~N & SO L YO M , 19R (,) 
\ ,cgl!lI lla : l =hll~ ()[i l1a RP . I : 2=buso[ill:l RP-2: J =bll.~olina RP-3: ·1=buSnliJl:.l flP -4 : 5=bu _(otill<l nr-s: 6=bll.~ul i l1a PP- I : 7 =hu sutill a PP-2 ; 

~=!.:d j lli cl1" Qd.:lIininlll : 1 00"~"i"!c .! .Ill 



this reseclirneillcd Jllaleria] can easily mix with other 

m;lIer i:1is. Undoubtedly. loess could have been blown 
directly to a sedilllen tary basin (lake, marsh, pond, 
river). \Vincl blown dust and sand contribute to the com­
position of various types or sedimen ts which ultimately 
accumulate in fluvial or subaquatic environments (EIN­
SELE. 1991). 

The heavy mineral composition shows that. COIll ­

p:-ncd to the younger units, Unit I is depleted ill its gar­
net content (Fig. II ). This almost complete lack of gar­

net can be rel:lI cd to the source area. [I' we assume dOIll­

inant loess origin of the unit , the difference ill garnet 
conlent GIll also be rei:lIed to transport. Namely, the 
lack of the heavier garnet, cOlllp,l recl to the much morc 
nounciant lighter epidote Ill;l)' imply that the source area 
W;lS silu;lIed far ,l\vay from the depositional basin. 

With the exception of the silty-clays, a dominant 
ch;l ractcri :-.t ic of Unit L at Jeast ill its upper part, is the 
predom inantl y yel lowis h-red and yellowish-brown 
appe:u",mce of tile sediment s. XRD-diffr<lctograms sho\v 
rh ;.lt the yellow ish-red mottled si lt y -cl~IY , situ;ued in the 
upper part of the unit in the drill core BP- I contains, 
among othe r minernl s, goelhite. The pr ese nce of 
goethite indicates th;lI the sediment has been ox idized. 
The occulTence of more than 10 III thick ye llowi sh-red 
sediment in pl<1ces may sugge:-.t that the colour of the 
sediment : (I) is original, implying that the sediment 
\vas depos ited in a well oxygenated environment , (2) 
rcflects pos t -burial, po st-llepo sitional oxid~lljon 

processes, (3) reflects post· depositional weathering. 
Togethcr, the yellowish -red 11101l1eo appe;Jr;Hlce, 

lack of carbonates and presence of goethite suggest til;H 
the upper part of the unit in the drill core BP-I was 
influenced by weathering, i.e. so il forming processes. 
Accordin g to RETTALACK (1990), the geornorphic 
se ttin g. of p:1laeoso ls may not always be obvious, but 
their relationship to the water table often is di scernible 
and has a clear bearing on their position ill the lnnd ­
SC1 pCS of the past. The presence of ye llow ish-red mot­
tles in the prcdomin;llltly grey silty-clay, noticed in the 
upper pan o f the unit in the drill core BP-4, indicate 
that the pa leosol (and underl ying sediment) had been 
partly within th e zone of welter table fluctuation. 
Com pared to the \vell drained yello\vish-red pal;leosol 
observed in the drill core BP-l, the grey onc contajns 
calcite, dolomite and smectite and lacks goethite 
(except in mottles). \Ve suppose that, during the wet 
seilson, pal<leosol was affected by gleying processes. 
During the dry season (lower water table), liberated fer­
rous iron was ox idi zed and fixed as goeth ite on yellow­
ish-red mottl es . It is necess;u'y to stress that the features 
implying waterlogged conditions were noticed at differ­
ent levels through the prevailingly yellowish-red Uni t L 
The origin of these features is disputilble. 

Allhough indi sputable evidence for the prevailing 
yellow ish-red appearance of Un it T is not available, 
existing fact s are suffic iently convincing and illlply thm 
at least the LIpper p;lrt or the unit represents a palaeosol. 
In additioll , waterlogged features may indicate that sev -

81 

eral st:lges of wC<ltherillg or post-buri;il processes were 
invo l ved. Nevertheless, the preserved ye l1O\v i sh -rcd 
appearance implies that oxidizing conditions within the 
unit were 1ll "1int;lincd bec;llIse little or no org;lnic J\l:lter 
or reducing pore waters were avail:lble to convert the 
iron from a ferric to felTous sl<lIe (ElNSELE, 1(91). 

According to KARLSTROOM (1991). much evi­
dence suggests th:1t 1;1Ie Tertiary and Pleistocene inter­
glacia ls in upper-ll1il1dle latitude continental reg ions 
were c1wracl crized by \\farm -tcmperate, sub tropical 
and/or Meditermne;lIl climates. At th;1I time, dirferent 
types of interglacial soi ls developecl. As palneosols gen­
erall y bem the imprint of the st rongest env ironment 
affecting their development (MORRISON, 1(78), we 
attribute the observed p(lleosol (lnd upper parts of the 
unit to be influenced by an interglaci;ll climate. 

The presence of pyrite and, pos~ibly siderite, as well 
as the grey colour of Unit II undollbtedly indicatcs that 
the sediment has been ;lllected by red llcing cOIHJilions. 
In addition, in drill core BP-5 the lower gravelly-s:lIldy 
interbed contains very well preserved wood fr;lgrnents 
with abundant pyr ite crystals. vVhile in the middle part 
of the unit limestone ;lIld dolomite pebbles can be 
found , in the sandy-gravels, in Ihe lower pan no pebble 
of carbonate compos ition li;lS beell observed. A charac­
teristic featllre of the unit is the presence of a l!Jlifonn , 
3.4 Il\ (IlP-1) to 5.5 III (DP-I) thick. grey s ilt y-sand 
which ove rli es the gr;lvelly interbeds . Although the 
upper P;1rt of unit is clwracterized by the silt dominated, 

fining upwards sequence, differences in colou r, thick­
ness and gr:lr1ulometric composition of the upperlllost 
part of unit , ll(ls been obser ved between cores. Gra in 
size pa r;lm eters of the lIpperm ost part of the lIllit (Fig. 
12) indicate loessoid sediments and a lacustrine-Illarsh 
type deposi tional environment. 

In Ihe drill core BP-I, tile uppermost part of tile unit 
in decreasing vertical oreler is cOlllljosed of yellowish­
bro\\!11 1l10ttled clayey-silt wi lh carbonate concretions, 
underlain by grey clayey-silt wit h yel low ish-brown 
mottles. carbonate co ncret i ons and rell1n;lnts of 
Rhisoconcretions, and greenish-grey clayey- silt with 
carbonate concret ions . T he clay content decreases 
dOW!IW(lJ"(ls. 

The vertical section described, and features men­
tioned strongly suggest tll;1I the upper part o f the unit 
was subjected to water - table tluctllmions. vVhile the 

ye llowish-brown mottled clayey-silt <lccompanied with 
carbonate concretions resembles well drained soi ls , the 
underlying grey clayey-silt with ye llowish-brown mot­
tles and carbonate concretions indicates seasona lly \vet 
conditions. According to EINSELE (I (91), carbon:lte 
nodules originating from near surface carbonate disso­
lution and reprecipitation are sillli1m to the formation of 
caliche. RETALLACK (1990) stated that ca lGlreous 

. concretions are thought to have accumulated under 
alkaline conditions of dry period s. Rhisoconcretions 
(observed in grey clayey-si lt) form in soi l s because of 
the spec ial local environment created by roots 
(RETALLACK. 1990). As the result of re peated cycles 



82 

of wetting and drying, roots may become heavily 
encrusted with concentric layers of very-fine grained 
low-magnesium calcite. The presence of Rhisoconcre­
tions suggest that the sediment WLL~ subjected to repeat­
ed cycles of wetting and drying. Although the appear­
ance of carbonate concretions can be attributed to the 
same phenomenon, their possible diagenetic origin can 
not be neglected. Nevertheless, the fact that yellowish -
brown mottled clayey-silt undoubtedly developed 
above the water table indirectly implies that it was sub­
jected to soil forming processes. 

Unit [[ probably developed in a shallow, oxic lacus­
trine to marshy environment with periodic fluvial influ­
ence during the lower and middle parts of the unit. In 
the upper part of the Unit, loess conn·ibuted to the local 
material. As a result of increased sediment supply, or 
reduced subsidence, or changing climate, the sedimen­
tary basin became a seasonally dry marsh (tluctuating 
water table and gleying phenomena) which successively 
dried up (yellowish -brown mottled well drained appear­
ance). In the drill core BP-4, the greenish-grey sandy 
clayey silt with sporadic pebbles, irregularly distributed 
calcite, possible siderite concretions, and lack of yel­
lowish-brown mottled appecmlllce can be attTibuted to 
processes of burial diagenesis. RETT ALACK (1990) 
states that a serious complication for the interpretation 
of seasonality in swamp soils is the tendency of such 
lowland regions to be slowly subsiding sedimentary 
bas ins. As a result, a seasonally dry swamp may sub­
side below the water table to become a permanently 
waterlogged soil. Tn addition, soil can be strongly 
reduced upon burial and subsidence into a biologically 
active water table. 

While in drill core BP-I, the boundary of Unit TIl 
with the underlying unit is emphasized by a marked 
change in colour, in the drill core BP-4, the contact is 
sh~up and marked by an abrupt change in granulometric 
composition and slight change in colour. 

In drill core BP-l, the lower pmt of the uni t is COIll­

posed of greenish-grey sandy-clayey silt to clayey-silt 
with sporadic plant remains. The grain size parameters 
(Fig . 12) of the greenish-grey sequence suggest a loes­
soid origin. The lower part of the unit in the drill core 
BPA is composed of an ungraded , sand dominated mix­
ture of gravel, sand, silt and clay. Such a latera.! differ­
ence can possibly be attributed to the position in the 
sedimentary basin, probably related to the proximity of 
land or a tluvial inflow in the sediments of Unit III 
(drill core BPA). 

The greenish-grey to grey colour, accompanied by 
plant remains (e.g. BP- I) and p)1·itized wood fragments 
(e.g. BPA) together with a lack of carbonates, strong ly 
suggest that the sediment was developed in a reduc ing, 
acidic, probably marshy environment. The presence of 
ostracodes and remains of Lifhoglyplllls in the grey 
sandy silt above the marshy, greenish-grey clayey-silt, 
indicates a fresh water inflow, which resulted in the less 
acidic conditions necessmy for the preservation of cal­
cite and dolomite (in drill core PP-2) , 

Geologia Croatica -16/1 

Above the fossiliferous grey sandy-silt is a yellow­
ish-grey to grey si lt y -sand, over la in by yellowish­
brown mott led silty-sand pa laeosol. Furthermore, the 
upper part of the unit is characterized by the presence 
of greenish-grey clayey-sill in the drill core BP-4, and 
yellowish-brown clayey-silt in the drill core PP-2, both 
with the abundant cartxm<lte concretions. Observed lat­
eral changes, mainly related to colour and the pres­
ence/absence of carbonate concretions can be attributed 
to a f1ucculating water table , both, during pal:leosol 
formation and after burial. 

Unit TV is composed of s~Uldy gravels. We interpret 
this unit as a tluvial deposit. 

No distinctive conclusion on source material can be 
drawn from clay mineral assemblages (Figs. 13 and 
14). In clastic sediments of Pleistocene age, situated 
along the southern slopes of Mt. Medvednica, the main 
clay minerals besides illite are vermiculite and smectite 
(SLOVENEC & SIFfAR, 1991). Kaolinite is observed 
as well. While chlorites in low-metamorphic rocks of 
Mt. Medvednica were the minerals , out of which ver­
miculite and smectite were form ed during the weather­
ing processes, the problem of the origin of kaolinite 
remains to be resolved. 

Clay minerals in rnost clastic lakes are detrital and 
reflect the composition of the source rocks and there is 
no exclusive phylis suite (WEAVER, 1989). CHAM­
LEY (1989) stated that a general correlation ex ists 
between the mineral composition of most freshwater 
lakes and the average clay mineralogy of rocks and 
soils in the surrounding drainage basins. 

The use of clay minerals in pa laeosol investigations, 
with a view to a cl imate reconstruction, assumes that 
soils form in equilibrium with the climate. If such soils 
are subjected to the action of erosion, are transported 
and deposited in a sedimentmy basin (e.g. lake) , the 
reworked sediments will bear traces of th e mineral 
composition which actually expresses climate related 
weathering patterns. 

For example, kaol inite from the paleosol si tuated at 
the top of Unit I probably formed by the action of soil 
forming processes, during a warm , moist interglacial. 
In well drained conditions, kaoli nite is a stable mineral 
phase. During that period, kaolinite ~L'i a secondary min­
eral certainly developed on remaining continental sur­
faces . In subsequent periods , neofofmed soils were 
exposed to the action of erosion processes and undoubt­
edly contributed to the composition of younger sedi­
ments . Using this mechanism , a presence of kaolinite in 
the lower parts of Units II and I II cou ld possibly be 
explained. 

The fact that clay minera ls have an important role in 
these kind of investigations is obvious ly importa nt. 
Future investigations of the Quaternary sediments 
should include investigation of the c lay mineral assem­
blages in related sediments, palaeosols and potential 
source rocks, respectively. 

In order to evaluate the role of tec tonic events on 
the development of the recognized units, the fo llowing 



Velie & Dum: Altl~m:ltillg L:lCll~trille-YLrsh ... 

Illust be stressed. The morphology of the base surfaces 
of Units II, III and IV are mutually different (Figs. 8, 9 
and 10). In ascending order, they are more simple in 
appearance. When overlapped, maps in general show 
neither coincidence between uplifted nor depressed 
p;u·ts of the study area. This is, aillong others, a conse~ 
qucnce of neotectonic lIIovelllents. The area studied is 
situated at the mutual edge of two structures. West of 
Precko, an uplifted structure, which was active during 
the Middle and Upper Pliocene and Quaternary was 
recognized, while due e~L<;t, an inverse structure which 
subsided during the Pliocene and Quaternary was 
observed (VELlC, 1980). Local processes of tectonic 
uplift and subsidence were only partly compensated by 
sedimentation and denudation, respectively, which 
resulted in wnrping of the ba"le sUitaces. 

6.2. CHRONOSTRATIGRAPHIC 
RELATIONSHIPS 

lndex fossils were not discovered and radiometric 
age determinations and paleomagnetic conelation were 
not performed, which has resulted in the problematic 
chronostratigraphic affiliation of the units recognized. 
By placing all of the relevant data into a generally 
accepted paleoclimatic framework of the Quaternary 
(MARKOV, 1970; SEGOTA, 1966, 19(7), the follow­
ing chronostratigraphic characterization is supposed. It 
has to be ~tresscd, that during the investigation of strati­
graphic relationships we used the terminology for 
glacial and interglacial sequences of the Alpe regions 
regardless the serious relllmks concerning their scientif­
ic justifiability. Namely, the authors on papers deaJing 
with the Quaternary in Croatia exclusively used the 
cla .~ificatioll mentioned. In order to correlate our results 
with reslJ1t~ of adjacent areas, we used the same tenni­
nology. An identification according to the chronostrati­
graphic scale for Europe was performed after I-IAR­
LAND et al. (1990), especially in division on the Lower 
(Early) , Middle and Upper (Lote) Pleistocene, and after 
NILSSON (1983). 

The oldest Unit is Lower Pleistocene in age. Since 
of dominant loess origin, it is considered to have 
fonned during the Menapian (GUnz). This is also cor­
roborated by the position of the conditional marker 
horizon Q', which wa-; defined over a wider area of the 
Sa va depression (HERNITZ et aI., 1980) on the basis of 
logging, performed on cores from about a hundred loca­
tions around Zagreb, Sisak and Mt. Moslavacka Gora. 
This miU"ker separates the Lower Pleistocene from the 
Middle Pleistocene, Upper Pleistocene and Holocene 
sediments, as documented by URUMOVIC et al. 
(1976). Above the Q' marker, the "unconsolidated 
material" of HERNITZ et al. (l981) is situated, which 
is, compared to the underlying, fine-grained, semi-lithi­
fied, impermeable sediments, mainly composed of per­
meable strata. On the basis of described ch;'U'(lcteristics, 
it is possible to recognize the Q' marker on the well-log 

83 

traces which are shown on Figs. G and 7. Isopach map 
(HERNITZ et aI., 1980, Fig. II), showed that infened 
thicknesses between the Q' mmker and the ground sur~ 
face, in the area of Precko \vere lower than 50 Ill. Our 
results indicate that the maximum depth of the Q' 
marker is 40 rn (well BP-l, Fig. 7) 

Unit II is Middle Pleistocene in age. Contact with 
the underlying unit is sharp. In the lower part, Unit II is 
composed of grey, poorly sorted gravels and sands, 
deposited by running water entering a shallow lake or a 
marsh. We consider the lake formation to be related to 
the Holstein interglacial CMindel/Riss), during which a 
moist, warm climate prevailed. The granulometric and 
bulk composition gradually changes upwards with 
increasing silts and clays, possibly indicating, that the 
transport mechanism also changes, probably with the 
incoming glacial, possibly Saalian CRiss). During the 
mentioned glacial at least two w::U"ming phases occured 
and therefore the lacustrine-marsh type sedimentation 
was probably maintained until the very end of Saalian. 
The increased loess contribution, accompanied by 
mmked cooling and dryness during the last third of the 
Saalian glacial, resulted in long lasting aridity, 
Correlation with the results obtained in the vicinity of 
Podsused by VELIC & SAFfle (1991), also suggests 
the Middle Pleistocene age of Ullit II, as pebble litholo­
gies at both localities ;ue almost identical; sandstone 
and qualtz/quartzite pebbles being predominant. 

We consider Unit Ilf to be of Upper Pleistocene age, 
(predominantly Lower to Middle Weichselian). Panicle 
size analyses partly indicate a loess origin of the materi­
al. A marsh type environment is also documented. 
Marshes were possibly formed during the Upper prut of 
the moist and warrH Eemian interglacial (Riss/WUnn). 
Compared to the Holstein (Mindel/Riss) interglacia! , 
this was characterized by decreased humidity. Frequent 
lateral changes of lithological composition occur. 
Fluviatile gravels and sands, found in a small numbel 
of localities indicate the proximity of a coast line. In the 
upper part of Unit lIt varve were recognized in the 
field, as alternating millimetre thick, light-coloured, 
fine-grained sands and dark grey to black silts. They are 
a typical product of glacial conditions. Since the maxi­
mum Quaternary cooling began during the second half 
of the Weichselian (Wunn), these sediments are compa­
rable with the climatic conditions. 

It has been previously stated, that pyroxene was not 
found in the heavy mineral fraction of Units I, II and 
Ill. This is in agreement with studies by RAFFAELLI 
& MUTIC (1982), who concluded, that the lack of 
pyroxenes is a typical characteristic of the Upper 
Pliocene-Pleistocene sediments, compared to the Sava 
sediments of Holocene age. 

Unit IV is Holocene in age and of fluviatile origin. 
Well rounded pebbles of, predominantly carbonate 
composition, as well as the degree of sorting, COITe~ 
spond to the results, obtained from exploration wells 
situated slightly west of the study area (VELIC & 
SAFfIC, 1991). 



84 

Im ( 

I! 

BP- 1 
1 2 

,-, 
G 

B, G 

G 

B,G 

, , 
G 
G ~Gr 
c. -()r 

G- Gr 

G-Gr 

V-B 

GlfY -8 
G-Gr 
V-G 

V 

G 

G 
. . G ........ g 
--, 
~B'G 

G 
G 
G 

G 

G , 

y - " 

,- , 
y- " 
y -" 
y-" 
C."Y- R ,- , ,- , 
Y-R 

G 

3 4 5 6 
/"/. ) 

0 20 " 60 , , , , , 

-= M ,O 

~ 

... !l <> 
_ o R 

0 

... n .. ~ ? : 

Ilg IJ C,)rr~ la l ion of rc:;ults of fidd anu [:lbumtury investigations, wdJ RP- I . 

S1. 13 Knrdacija rc1.Ll lt :lla l ~r.:nski h i lablJr:llorijskih islrai.ivanja , bu;:;oIina 01'-1. 

(wi "I.) 
OJ 100 

* 

* 

* 

111 Oo0 ~o l 12 0 13[8 ~ 210 1.4 ~ oOe o ~ ~ 

7 B 
{ "/01 

0 '" " '" OJ 100 ~.ioIaIJJIj.Ud~·1 , , , , , , , , , , 

r-----i * ftt-m-f1!!t/Wi 

* • • • 
111111111111111111 *... .. 

* • • 

* • • 

9 

IV 

III 

III 
II 

II 

22~ 23~ 2 '4~ 

25[G- Gr l 2,6B 2,7 [GgY-BI 2,a [ Y t B I 
Y - R 29~ 2,10 [GlI'Y-Rj 31

0 
3,2 0 

330 3.40 3,5 [, "I 36[ , I 3'7@J 3,a~ 39[ @ I 41 [c::J1 
42[1 ? 'I 5,1 5,20 5,3 

( - ( 
5,4 D 61

0 
6,2 63 

64 6,5 6,6 0 67
0 6,aD 7 1 7,2. 73 D 

al~ 8,2B 8,3 B 8.40 8,5 0 8,60 8.7B 88 [2] 

89 8 8,,00 8''' 0 8,,20 8 , '3~ 91~ 92QiD 93 0 
94[JJ ,0" 0 

l.A:gcnJ for Figs. \3 and 14 . 

i..cgcmb J;;J slik.:! l ?o i 14 



Veil'; &. 1)11n!: Allenl;\lllIg L':II.:\J~lrlll<,· '\1:! r..h .. 

1m ' 

BP-4 

1 2 

, .. 
B-O 

o 

Y'G , 
y. , 

o 
o 

o 

, 
o 

G-Gr 

o 
, 
o 

o 

o 

G 

Y-Gty-R 

Y-R 

Y- R 

3 

<> 

= 0 

<> 

0 

.. 

.. 

.. 

4 

= 

n 
'? ' , . , 

n 
: ? ~ 

5 

Fig. 14 Corrl!Luiutl nf r~':.I1 I( ~ of fidJ ano laboratory invl!sligaliol1s, wdl I3P-4 . 

6 

SI I'; K{Jr.:I;H:ija r~ndtala kn.:n:-kih j laboratorijskih is(r;Jzivanja, bll ~v(j!la I3P-4. 

1. Lithology: 1.1 ):r;lvd: 1.2 =~;mJ: 1.3=silt: 1.:I=1:1:Iy 

7 8 

* 1111111111111 

* •• • 

* ... 

*. 
* 

* • 
*. • 

* ' 1 

• 
• 

• • 

85 

9 

IV 
III 

III 

II 

II 

2, Colour: 2.1 ,L:fI')': 2.2_ briglll grt,y; 2.3=brownish gn:y: 2.:1 =ycllowish !:In:)'; 2.5=grcyi~h green; 2J'=yd lowish brown: 2.7=grl'y 3110.1 ),l'Ilowi"h brown: :U~ ydow 
i~h 8f{')' :\Jld ),"lIowish rc<.t: 2.9 ,=- yc ll owi.~h n:J; 2.IO=gre)" :md ),ellowistl red 

3. P.:il:l\·oulnlo)o:il':11 ,~)111bo[s :md soil· fonning/after lxlri:ll ft::J.ll1res: 3.1 =11Iohl.~C3 fr'lglllcl!t~; ].2=oslr:lcOl\s: 3.3 Rhi zocolll:rctions: 3.4"'I'I:lI\t rr:lg\\Wllt~: J.5 -= wood 
fr.18r1lCllts: ]J;-=mnuks: 3.7=pyrite: 3.8=C3kt:rolJ~ I:o[](;n:liolls: 3.9=limonitizl'J 1'")<.:k fr:1811ll:1l1 

4. lolH'S wilh t"t-:IIUI"\.'S "hi..:h jndicile pos..<ible soil fomling pro<,xsSes: 4.I=p:\l;h'n~nl; 4,2 =1lI\ddcnl\ilH~d lower OOIU1J.:IrY of:l l'aL:H~osol 
5. Gr.Lin si1e di~trilxltion: S.I::::gr:wd; 5.2=s:lIld: 5.3-,silt: 5.4 -1:13), 
Ii. Gr:.lvcl<.:oml'n~iti()I\ (gr;l/mlc~ :lIld pI;bbks): 6.1 =limt:Stom:.~: 1l.2=doloSIOllcS; 6.3 sallds !on'l~; liA"'qllartl.i!es: {'.5=.:x!nlsivc rock.~ and tuff: 6.6=cOlIglOtlll:r:I!C~ 

311,[ br"cci:ls: {,.7=chcrt: 6.8",othcr rocks 
7. SdCl'lcd hc~vy l\linerJ.t~ ralios: 7.1 =gamd: 7.2=epi,toIC: 7.J =l.in:Olll tOllnn:tlille 
8. MiI ICr:tI<)gi~·~I..:<)mposilion of d~y :md silt rich mat{:n3Is: 8.1 =,Iolnmil": 8.2=ral<.:i le; 8.3= uniJclllifi.-d ":3rOOIl:lle miner-II (pmsibly sidcrite): 8.'1-:tIUat1z: 8.5=pb 

giocl:lsc: 8.f, ..., fdd.'p:tr: 8.7=go<;lhilc: S.8 mica: 8.9=chlorit.·: 8.IO-Mllectitc: S.II =mi:lt:d-bYl:r cby IHiner:lls; S.12=k.:lolinit.:: S.13=i.klllificd milwml..:on~tiluent 
9.ldmtified IIntls: 9.I .:.UniI IV: 9.2 _Ul\it III: 9.3 =UniI 1l : 9.« ::::Unit I 

10.1 =- I-'ositillll 01':1 s:lIllple. 

I. ulolo;kl S:I~I~V: 1.I=sljull:t.k; 1.2=pijt:S.:lk: I.J=si1t: 1.4::::glina 
2. n oj:1 n~~I~g.,: 2.1=~ivo: 2.2:::svij<'llosivo: 1.3~mcJe'<ivo: 2.4=i\\':bsto~ivo; 2.5 - sivk:ll>toze1cno: 2.(, ·zui·kastosrnede: 2.7 sivo i 1.\Jck:I.~lo.~mt:tk: 2.8=1.W;bslosi 

vo i lu":k.1stO<.:rv .. uo: 2.9=F.tI";k:!slocrvetlo: 2.IO=sivo i zutk:!stocrveno 
3. P3lconotolo~ke owake i I'cUogel\dske/dij:lgcoct.:,ke poj~ve: 3.1' fr:lgnH:llti Ij\J~Ulr;J IIlckll.h,:a: 3.2=ostr;lkoJi: 3 . .i e rizokonkn:cijl:: J.<1=biljno tnmj,': 3.5 =oSllCi 

drvet:!: 3.6 .... bn:: J.7=pirit: 3.8""brlx)[J3Ine konkrecijc: J.9=fr:J/91H:ll li lirnnnilizir:luih stijen:l 
4. Zone ~ pOj.1V:l!l1~ kl)jc llknuju n:! pTOc,~~e stV:lr.l1lja tb: 4,I=p:l lcotlo; 4.2 p~kl)llo txZlIlvrdcnc d(Jllje gr:mice 
5. GrJllulnlllclrij~ki ~;l~tav: 5.1 =sljunak: 5.2=pijes~k : 5.3=si It: 5.4=glil1:t 
6. I\'trngr:lf~ki S:ISt:1V v:llutil:3: 6.1 =V"[lIlCrl:JC: 6 .2=d(Jlor!lil; 6.3 =p jc~ccnj:\k; 6.4 k v:trl:it; 6.5=cfllzivi j tllf: 6.6=kof18JolllerJti i brcce; 6.7=ccr'l: Ii. S o~1:\I.: stijt:ne 
7. O.ll\1)S iz:il)r.11I ih h'skih lIli lIerala: 7.1 :- gr:ln3t: 7.2=epidol; 7.3 =<.:i rkon + tunllal ill 
8. Min<'f:t ini ~':I~tW gli!1.~ i siltova 8. J=dololl1 il; 8.2=blcit; 8.3 ncd<:finir:H1i brbollat (vjcrojatno sidt:ril): S.4=kv:lre: 8.5=p l a 8i()kla~; 8.6=fddsp:,I; R.7=gctit: 

8.8"'"- tinjci: 8.9 kiorit: S.IO - Sll1ektit: 8.II =mijdilno·slojni !l1 iner3 ii glilt3; 8.12=k:\ol in it; 8.13=ident ificir:mi miner;)l 
9. Iblluc<'ll<' j(:dinicc: 9.I =jcdinic:J.1 V: 9.2 ::jedinica llf: 9.3=jcJinicall; Q .... ·.::jcdini<.::t r 

lO.I =Pnlobj lIZOrk:l. 



86 

Overlying palaeosols indicate phases of subaerial 
exposure. Units II , rn and IV overlie palaeosols, indi ­
cating that the uppermost pmls of Units I, II and III 
were exposed to the act ion of pedogenesis. Three 
palaeosols occur in a 60 In thick interval of sediments. 
While the oldest palaeosol displays the greatest thick­
ness (in some cores more than 10 meters), the youngest 
is the thinnest , ranging in thickness from 0.1 to 0.7 In. 

Their formation is closely related with palaeoclimatic 
conditions implying that warm periods of specific 
humidity and duration are required. Since the differ­
ences among interglacial mean annual temperatures are 
relatively small (EMIUANI & SHACKLETON, 1974), 
the differences in paJaeosoi thickness were undoubtedly 
intluenced by the duration of sediment exposure to soil 
fomling processes. Nevertheless, it has to be stated that 
some authors assume that strongly developed pre­
Wurm paleosols fanned under long intervals with cli­
mate similar to the present (e.g. BOARDMAN, 1985), 
whi le others (e.g. KARLSTROM, 1991) find that the 
mean temperature and precipit.:1.tion during formation of 
the paleosols was at least 6-8°C wanner and 40 Clll 

higher than present. During approximately 200,000 
years of the Cromerian and Elsterian, almost the com­
plete drilled interval of Unit I was subjected to the 
action of soil forming processes. In the Eernian inter­
glacial , which lasted slightly less than 100,000 years, 
up to 2.6 m of the uppermost P'U1 of Unit II was affect­
ed by pedogenesis. A palaeosol, approximately 0.5 m 
thick, formed in the top Palt of Unit III , during the peri­
od of 4000 to 6000 yem's in late Weichselian and, possi­
bly, early Holocene. 

7. CONCLUSIONS 

On the basis of performed field and laboratory 
investigations accompanied by natw-al-gamma radioac­
tivity measurements four units are recognized (Figs. 6, 
7,11,12,13 and 14). Unit I is predominantly composed 
of yellowish-red, yellowish-orange and yellowish­
brown, poorly-moderately cemented, dense, clayey­
silts/silty-clays. Sporadic lenses and interbeds of grav­
elly-sands, up to a few dm thick also occur. Highly 
variable coefficients of sorting, compared to the aver­
age values (Fig. 12) possibly indicate that loess, mixed 
with local materials (Ioessoid) has contributed to sedi­
ment composition. The almost complete absence of gar­
net may be a consequence of aeolian transport. Unit J is 
Lower Pleistocene in age and is considered to have 
formed during the Menapian. This is substantiated by 
the conelation between the conditional marker horizon 
Q and the unconformity which separates Unit J from 
Unit IT. Tn addition, earlier investigations showed that 
inferred thicknesses between the Q' marker and the 
ground surface, in the area of Precko were lower than 
50 m, while, according to the present study, the maxi­
mum val ue is 40 m. 

Unit II ranges in thickness from 10.35 to 24.3 m 

(kologi;] Crrntica 46/1 

(Fig. 3) and is interpreted to be Middle Pleistocene in 
age. The unit is relatively uniform in composition: 
while the lower and middle p~u·t is predominantly COTll­

posed of grey coloured sands, the upper part comprises 
grey coloured or red to yellowish-brown mottled silt 
and clay sized material. Comse-grained sediments in 
the lower and middle part of the unit are poorly sorted. 
The high matrix content indicates that they were r~lpid­
Iy deposited in a quier-water environment i.e they were 
deposited from running water at the point of entry into 
a shallow lake or a marsh. The lake was formed in a 
humid climate, during the Holstein interglacial. With 
the incoming glacial, possibly Saalian, the granulomet­
ric and bulk composition grad ually changes upvv'ards 
indicating that the transport mechanism also changes. 
As the result of increasi ng loess accumulation aCCOIll ­

panied by a marked cooling and dryness, the 
lake/mm'sh dried out. 

Unit III is heterogeneous and ranges in thickness 
frolll 6.15 to 13.2 III (Fig. 4). The unit is characterized 
by frequent lateral changes of gravels, sands, si lts and 
clays. \Vhile the sands are predominantly grey 
coloured, the silts and clays are often mottled in yel­
lowish and brownish shades. In the upper part, v;uve 
are recognized , as alternating, millimetre thick light 
coloured, fine-grained sands and dmk grey to black 
sills. While particle size analyses partly indicate a loess 
origin of the unit, some recognized features suggest 
that the sediment was accuTlIulated in a marsh type 
environment. Resumption of a quier and shallow water 
environment cOlTesponds with the upper part of the 
moist ;Uld warm Eemian interglacial. Consequently, we 
consider Unit III to be Upper Pleistocene, principally 
Lower to Middle Weichselian in age. 

Unit lV varies in thickness from 6.6 to 7.7 III (Fig. 
5) and is Holocene in age. It is composed of pale, yel­
lowish-grey coloured gravels and sands in which lime­
stone cobbles prevail. 

The upper parts of Units I, II and III were exposed 
to the act ion of soil forming processes during ph,llles of 
subaerial exposure. At least three zones with palaeosol 
characteristics were recognized. The criteria used to 
recognize the palaeosols were: (1) different colour 
compmed to the overlying and underlying material, (2) 
presence of mottles, (3) presence of concretions and 
nodules, (4) evidence of weathering of minerals 
(goethite) and (5) presence of roots and organic matter 
fragments. These zones are closely related to the 
observed unit bound;u·ies. While the oldest palaeosol 
(Unit I) displays the greatest thickness (in some cores 
more then 10m), the youngest paleosol (Unit III) 
ranges in thickness from 0.1 to 0.7 m. Their formation 
required warm periods of specific humidity and dura­
tion. We consider these periods to be related with the 
Cromerian and Elsterian, Eemian, and late Weichselian 
and, possibly em'ly Holocene respectively. 

The occurence of both specific sedimentary envi ­
ronments and phases of subaerial exposure was also 
influenced by tectonic processes. The morphology of 



Velie & DlIm: Altemating l ..ac\l~trinc· M1.rsh ... 

the base surfaces of Units ll , III and IV are mutually 
different (Figs. 8, 9 and 10). In ascending order they 
are more simple in appearance. This is, among others a 
consequence of neotectonic movements. Namely, the 
tl rea studied is situated at the mutual edge of two struc­
tures which have been active till Quaternary. Local 
processes of tectonic uplift and subsidence were only 
partly compensated for by sedimentation and denuda­
tion respectively. 

Acknowledgments 

The au thors would like to thank B. Lugov ic, D. 
Slovenec and J. Tislj:u for allowing them to use the 
results of their laboratory analyses. Thanks al so go to 
Z. Blazevic, G. Hubeny, Z. Paladin and B. Sladovic, 
whose understanding, supon and interest enabled the 
performance of in vestigation works. The precious and 
patient assistance of B. S\adov ic during field -work is 
gratefull y acknowledged. 

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RAFFA ELU , P. & MUTIC , R. ( 1982): Mogucnost 



s. 

razdvajanja asocijac ija teskih minera la primjenoll1 
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smekl it 1I klaSlicn im sedimenlima juznih ol>ronaka 
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senschaft liche Geographie, Bon n. 20, 11 0-11 8. 

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SIKIC. K. & BASCH. O. (1975): Geoloska zbivanja od 
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za naftu JAZU , Zagreb, Al5, 69-86. 

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J. ( 1976): 0 propusnom mediju kvartarn ih Ie gorn­
jo- i srednjopliocenskih naslaga sjeverne Hrv<l tske.­
Zbornik radova 4. jugos l. simp. 0 hidrogeo l. i inz. 
geo l. . Skopje , I, 395-4 10. 

VELI e, J. ( 1980) : Geo loska gral1a zapadnog dijela 
Sav ske depres ije. - PhD T hes is. Ull i ve rsity of 
Zagreb. 137 p. 

VELIe, J. & SAFTI C, B. (199 1): Subsu rface spread ing 
and fac ies char"lcteristics of Midd le Ple istocene 
deposits betwee n Zapresic and Sarn obor.- Geo!. 
vjesnik. 44. m -R2. 

WEAVER , C.E. ( 1989): C la y. Muds , a ll d Sha les .­
Elsev ier, 8 19 p. 



Veli,,; & Dum : Al1<:m~lillg Lacllslrillc M:H~h ... 

Izmjena jezersko-mocvarne sedimentacije i kopnenih faza tijekom kvartara na lokaciji 
i'recko (Zagreb) 

J.Velie i G. Durn 

Na lokacij i Precko povrsine od 6 ha (s l. I ) proueene 

su talozine u prvih 60 III dubine. Izradeno je sedam 
bllsoti na; cet iri na lijevoj i tri na desnoj obaJi Save (s1. 
2) . Izvuceno j e ukupno 390 III jezgre. One su na terenu 
determinirane te je prikupljeno i vise desel.aka uzoraka 
za laboratorijskll i kabinetsku obradu . U busotinama su 
obav ljena geofizicka snimanja prirodne i izazvane 
radioaktivnosti. 

Tijekom st udiranja stratigrafskill odnosa djelom ice 
su koristeni nazi vi gl8cijalnih i interglacijalnih sekven­
cija za podrucje Alpa bez obzira na ozbiljne primjedbe 
gledc njihove znanstvene utcmcljc!losti. Naime, au tori 
kvartaroloskih radova 0 terenirna Hrvatske rabili su 
iskljucivo spomenutll klasifik(lciju pa smo korelirajllCi 
!lase s rezultatima za sllsjedna pocJrucja i Illi Illorali tako 
postupiti. Jdentifikacija s kronostraligrafskom skalom 
za Europu obavljena je prema HARLAND el al. (1990) 
- n(U"ocito 1I podjeli na donji (rani), srecinj i i gornji 
(kasni) pleisloce ll , Ie prema NrLSSON (1983). 

Na temelju sv ih terenskih i laboratorijskih poclata­
ka te prosjec ne prirodne gama-radijacije (s1. 6, 7, [I, 
12, 13 i 14) razlucene su cet iri jedillice. leciillica T 

izgradena je pretezito od poluvezanih, gustih glinovitih 
silt ov a/s iltoznih glina karakteristicne zutonarancaste 
(crvcne) iii zlJtosmede boje. Sporad icno SlI prisulne Ieee 
slj unkovitih pijesaka debljine nekoliko decimelara. 
M,llo povisene vrijeclnosti koeficijenta sortiranja u 
oclnosu Il<l srednje vrijednos li (s1. 12) ukazuju cia se 
vjerojatllo racli 0 Icsu pornijesanorn s lokalnim materi­
jalolll (lesoid). GOIOVO potpuna od sutnost granata 
Illoguca je posljedica eo 1skog transporta ce stica. 
Spomenuti krupnozrnasti klastiti ukazuju pak i nn 
donos vodama tekuciclllna, najcesce blljicama lJ plitkll 
slatkovodnu sredi nu. l edinica je donjopleistocenske 
stllrost i. Pretpostavlj~lmo cia je nastala tijekom menapi­
;lna (glinz). U prilog takvog tllrnacenja lib raja se i podu ­
daranje kroville ove jeclinice s llvjetnim reperom Q' kao 
i ranijim iSlr:-lzivanj irna pretpostavljene debljine stijene 
od repenl Q' clo povrsine terena - manje od 50 m, ovdje 
konkretno oclrc(1eno 40 Ill. 

Jedinica II debljine 10,35 do 24,3 III (s l. 3) inlerpre­
tir:ma kao srednjeplei stocenska, j ednolicnog je sastava: 
II donjclll i srednjern su dijelu uglavnolll pijesci sive 
iJoje, a u gornjem sve vise irna si ltova i glina, sivih iii 
"sarenih" s rnrijailla crvene do zlitonarancaste boje. 
Krupnozrnasl i kJastiti donjega i sreclnjega dijela lose Sll 
sortirani. Visoki ucljel glinovito-siltnog matriksa u 
njim<l ukazuje da su taJozeni u uvjetirna brze sedi ­
mentacije u vodenoj sreclini niske energ ije, tj. da su 
nastali akumulacijolll iz voda tekucica prigodom lltoka 

u jezero iIi moevarll. lezero je fonn irano u mladem 1101-
steinu (m illclel/r iss interglacija l) zahvaljujuci prven ~ 

stve no humidnoj klimi. S nastupanj e glac ijala saal e 
(riss) postupno se mijenjao sas ta v, vel icina i nacin 
donosa cestica, tj. sve je izrazenija i akllillulacija lesa, 
5tO je uz zahladenje i SUSll prouzrocilo presusivanje jez­
era/moevare. 

ledinica 111 karakteristicna je po heterogenom sas­
tavu i varijacijama deblj inc - od 6.15 do 13,2 III (s1. 4). 
Radi se 0 cestirn boenim izmjenarna sljullaka, pijesaka, 
siltova i glina. Pijesci su IIglavnolll sivi , a siltovi i gline 
testo mrljasti u nijansama zute i smet1e boje. U gornjem 
Sll dijelu uocene varve: milimetarske iZl11jene svijetlih 
silllozrnastih pijesaka i tamnosivih do crnih silt ova. 
Prema veJicini cestica ova je jedinica clominantno 
lesnog podrijella s obiljeij ima geneze II 1l10cvarnoj sre­
ciilli 5to zll;lci i unosa detritusa voclenirn Iransportoill. 
Obnavljanje mime, plitke voclene sredine u korelaciji.ie 
s vlazn im i toplim interglacijaloll1 eern (riss/\viirrn) i to 
njegovirn mladim dijelolll, dok je seclimentacija razrna­
trane jedinice gornjopleistocenske, pretezno starije do 
sreclnjoweichselske (wLinn) st;u·osti . 

Debljina jedinice TV krece sc oct 0,6 do 7.7 m (s l. 5). 
Radi se 0 holocensk01l1 sljunku i pijesku svijct le 
zLlckaslosive boje, stancJarcinog petrografskog sastava 
savskih nanosa kcxl kojih su dominantne valutice vap­
nenaca. 

Vrsni clijelovi talozina I, II i III jedinice bili su 
izlozeni procesirna pedogeneze. Ustanovljena Sll barem 
Hi nivoa sa znacajkarna paleotala. To Sll ZlI tO ­
narancasta-crvena-smeda boja nasJaga, prisutnost mrlja 
iii sara , konkrecija , nodula, korijenja te Illinerala 
trosenja (get it). Odnosni Sll nivoi usko povezani s grani ­
cam a medll jedinicama. Razlieito su izrazeni. 
Obuhvacajll od preko 10 m (jedi nica T) do 0,1 m 
Uedinica Ill ). Za njihovo je stvaranje bila potrebna 
lopla klima odret1ene vlainosti i trajanja, cem u odgo­
varajll intervali od cromera clo holsteina, zatirn raniji 
eern i naposljetkll kasni weichsel s eventual no starij im 
holocenoTll. 

Na genetski tip naslaga j pojavu kopnenih faza utje­
cali su lakoder i tektonski procesi. Oblici podinsk ih 
ploha jedinica II, III i IV (sl. 8,9 i 10) uglavno se 
medllsobno ne podlldaraju , a icluci prema mladima 
razlucene jedince se rasprostiru llIlutar sve manjih 
visinskih intervala. To je posljedica razlicito izrazenih 
10ka lnih spllstanja i izdizanja u rubnirn zonam<l 
nasljedne (na zapaclu od Preckog) i inversne (na istoku) 
strukture, aktivnih do u kvart~u· . Tektonski pokreti su 
oci to sarn o djelomice kompenzirani seclimentac ij om, 



90 

odnosno denudacijolll. 
I na kraju, ali ne i manje vazno, jedna pripomena. 

Kako bi se izbj egJe nedoumice, a omoguc ile strati ­
grafsk e usporedbe s Europskim i sv j etsk im 
post ignuCim3, ubuduce sv akako tre ba pred vidjeti i 
obavljat i rad iometrijske analize (osim testa prilllijenji ­
va nu rad iok arbonsku metodu i mj erenja na bazi 
dugozivucih radionukleida) uzoraka kV31tamih ta loiina 
s terena Hrvatske kao i paleomagnetne korelacije. To je 
jedini nac in da se dode do kriterija za valjanu i opeepri ­
hvallj ivu kronosU-at igrafsku klasifikaciju _ 

GeQlogia Cro.1ti(;:l. 4()!1 

Autori zah valjuju B. Lugov icu, D. Siovellec li i 1. 
Ti sljaru SIO su dopustili kori stenje nj ihov ih laboratori ­
jskih analiza. Vel iku zah va]nost takoder treba izrazi ti Z. 
Blai.ev ic, G. Hubenyu, Z. Palacl inu j B. S laciov icu pora­
di razumijevanja, potpore j inte resa bez cega ne bi bilo 
moguce obavljanje predloienog programi:! istrai ivackih 
radova. U te renskoj fazi se osobitolll suraclnjom iskazao 
B. S iadovic, zbog cega mu pripada poseblla zahvala. 

Manuscript received December 12, 1992_ 
Rev ised manuscript accepted March 5, 1993_