www.geologicacarpathica.sk
GEOLOGICA CARPATHICA, APRIL 2010, 61, 2, 147—162 doi: 10.2478/v10096-010-0007-2
Introduction
Fluvial deposits are the principal source of information re-
garding terrestrial processes. Modern fluvial sediments partic-
ularly in industrial areas provide numerous data about the
impact of human activities on natural systems. Changes in flu-
vial and sediment discharge, the availability and character of
eroded material and anthropogenic material production are
obliterating natural environments and their characteristics.
The content of hazardous components/pollutants represents
strategic information for the quality of environment and sedi-
ment management. Whereas some of these components
(DDT, POP’s) are clearly anthropogenic in origin, certain oth-
ers (heavy metals) can be both natural and anthropogenic. In
such cases, not only the information on concentration of com-
ponents but also their source, represent the principal informa-
tion for environmental studies.
The provenance of clastic sediments includes all aspects of
the drainage area (source lithology, topographic relief, cli-
mate, transport energy and deposition environment hydrody-
namics), although the source lithology is the most important
parameter (Johnsson 1993; Sensarma et al. 2008). The data
obtained by the provenance analysis of the sediments is main-
ly used for: i) information about weathering processes, ii) dis-
criminating the paleogeographic and tectonic context of the
deposition, iii) describing diagenesis conditions, iv) high-
lighting differences between individual depositional units
(McLennan et al. 1993; Young & Nesbitt 1998; Singh & Ra-
jami 2001; Zimmermann & Bahlburg 2003; Passchier &
Modern fluvial sediment provenance and pollutant tracing:
a case study from the Dřevnice River Basin (eastern Moravia,
Czech Republic)
SLAVOMÍR NEHYBA
1
, MARIE ADAMOVÁ
2
, JIŘÍ FAIMON
1
, TOMÁŠ KUCHOVSKÝ
1
,
IVAN HOLOUBEK
3
and JOSEF ZEMAN
1
1
Department of Geological Sciences, Faculty of Science, Masaryk University, Kotlářská 2, 611 37 Brno, Czech Republic;
slavek@sci.muni.cz
2
Czech Geological Survey, Geologická 5, 150 00 Prague 5, Czech Republic
3
Research Centre for Environmental Chemistry and Ecotoxicology, Masaryk University, Kamenice 126/3, 625 00 Brno, Czech Republic
(Manuscript received June 15, 2009; accepted in revised form December 11, 2009)
Abstract: Modern fluvial deposits of a small fluvial system were studied in the area of eastern Moravia (Czech Republic)
with the aim of determining the provenance of the deposits and weathering processes. Identification of the source rocks
and their alongstream variations were used for the evaluation of the natural or anthropogenic source of the heavy metals.
Paleogene flysch sandstones, flysch mudstones and Quaternary loesses represent source rocks and reflect both the role
of recycling and local sources. Provenance from sandstones dominate upstream whereas mudstones represent dominant
source rock in the downstream part of the fluvial system. The contents of Pb and Zn are highly enhanced when com-
pared with the natural background in the entire study area. Their anthropogenic source is connected with the rubber/
shoe manufacturing industry and traffic. The contents of Cr, Co, Cu, Ni and V are usually lower in modern deposits than
in the identified source rocks.
Key words: Quaternary, heavy metals, natural and anthropogenic source, small river system.
Whitehead 2006; Borges & Huh 2007; Barbera et al. 2009). In
addition, the application of the techniques and methods of
provenance analysis can be used for the evaluation of the natu-
ral or anthropogenic origin of possible mineral components
and their fate in the deposition system.
The majority of provenance studies are focused on large riv-
er deposits. Since large rivers often drain highly variable
source rocks and their deposits reveal a complicated rework-
ing history, the precise recognition of the source rocks could
not be obtained unequivocally (White & Blum 1995; Nesbitt
et al. 1996; Sensarma et al. 2008). For this reason the present-
ed study is oriented to a small river system that drains few
rock types, so that the nature of the source material is better
constrained. The textural, mineralogical and geochemical
composition (major and trace elements) of the modern fluvial
sediments were compared with possible source rocks in or-
der to obtain information about: i) the provenance of the
modern deposits, ii) the weathering processes in the source
area, iii) the distribution/redeposition of the eroded material
within the fluvial system, iv) the natural vs. anthropogenic
source of the heavy metals.
Geological and geomorphological settings
The study area is located in the eastern part of the Czech Re-
public in the broader surroundings of the city of Zlín (Fig. 1).
The area is strongly affected by both agriculture and industry.
The area is mainly formed by deposits of the Rača Unit of the
148
NEHYBA, ADAMOVÁ, FAIMON, KUCHOVSKÝ, HOLOUBEK and ZEMAN
Magura Group of Nappes (Western Carpathian Flysch Belt
see Fig. 2). The Rača Unit (Upper Cretaceous to Oligocene)
is represented predominantly by the Zlín Formation, whereas
the deposits of the Soláň and Belověž Formations play a mi-
nor role. The Zlín Formation can be subdivided into the
Újezd and Vsetín Member. The Újezd Member (Late
Eocene—Early Oligocene) is characterized as rhythmic flysch
with predominance of arcosic sandstones and subordinate
beds of grey-green mudstones. The Vsetín Member (Middle
Eocene—Early Oligocene) is rhythmic flysch with dominance
of grey, calcareous mudstones with subordinate beds of fine-
grained glauconitic sandstones (Pesl 1968; Stráník et al.
1993). The Soláň Formation (Senonian—Paleocene) can be
subdivided into the Ráztoka and Lukov Member. Rhythmic
alternations of sandstone and mudstone beds are typical for
the Ráztoka Member. Rhythmic flysch with absolute domi-
nance of sandstones (arcoses, greywackes) and conglomer-
ates represents the Lukov Member. The Belověž Formation
(Paleocene—Middle Eocene) is represented by rhythmic de-
posits with a predominance of green-grey and reddish mud-
stones. Flysch rocks are often covered by younger deposits.
The areal extent of the Neogene clays is extremely limited.
The Quaternary sediments are more abundant, being repre-
sented by a wider spectrum of rocks. Loesses, blown sands,
sandy alluvial fans, anthropogenic, fluvial (muddy sands,
sands, sandy gravels), deluviofluvial, deluvial (muddy sand-
stones), proluvial deposits (muddy gravels) have all been
documented (Pesl 1982; Novák 1994; Havlíček 2001).
The erosive-denudation relief of the Zlínska vrchovina
Highland (the average height above sea level 354.2 m, the
average angle of the slope 6° 11’) was formed within the sub-
strate. Broad flat elevations and shallow widely open asym-
metric depressions are typical (Demek 1987). The relatively
broad river valleys are cut by numerous transverse erosive
short depressions with active small alluvial fans, ravines, and
slope instabilities (Jinochová 1996; Kašpárek 1997). The
Dřevnice, Bratřejovka and Lutonínka Rivers drain the area.
The smallest of them is the Bratřejovka River which springs at
an altitude of 520 m a.s.l. Its river basin has an extent of
32.1 km
2
with the average discharge at the river mouth being
0.31 m
3
/s. The Bratřejovka River flows into the Lutonínka
River at an altitude of 290 m a.s.l. The Lutonínka River
springs at an altitude of 540 m a.s.l. Its river basin has an ex-
tent of 89.3 km
2
and a course length of 15.3 km. The average
discharge at the river mouth is 0.89 m
3
/s. The Lutonínka River
flows into the Dřevnice River at an altitude of 245 m a.s.l. The
Dřevnice River springs at an altitude of 510 m a.s.l. Its river
basin has an extent of 434.6 km
2
. The length of the river
course is 42.3 km and the average discharge at the river mouth
is 3.15 m
3
/s. The Dřevnice River flows into the Morava River
at an altitude of 182 m a.s.l. (Vlček 1984).
Maximum discharges during the 10-year period were
195 m
3
/s for the Dřevnice and 21.7 m
3
/s for the Lutonínka
Rivers. The minimum discharge values were 0.14 m
3
/s and
0.02 m
3
/s, average discharge values 2.4 m
3
/s and 0.54 m
3
/s,
respectively. The actual daily values vary in orders of mag-
nitude of 3 to 4 during year. Daily discharge measurements
from the 10-year period (1997—2006) were acquired from the
Czech Hydrological Institute. The gauging stations are at
Zlín (Dřevnice River, close to the sampling site 8) and Vi-
zovice (Lutonínka River, close to the sampling site 3).
Strong seasonal trends and variability in discharges with
similar seasonal trend, that is noticeable differences between
spring and autumn periods can be found (see Fig. 3). Arrows
show sampling events in spring and autumn 2005 and 2006
that fall into typical periods with higher (spring) and low
(autumn) discharge stages. The differences between spring
and autumn periods are typical for rivers in drainage basins
in a humid climate, with maximum discharge values appear-
ing in longer periods following snow melting and in short
periods following summer thunder storm events.
Sampling and analytical techniques
Modern fluvial deposits were sampled at 9 sampling sites
(SS) located within the courses of the rivers Bratřejovka, Lu-
tonínka and Dřevnice (Fig. 1). The uppermost bottom layers
of the river bed (max. 10 cm thick) within the active river
channel were sampled manually over four successive sam-
pling seasons (i.e. May and September 2005 and 2006).
Combined sieving and laser methods were used for the
grain size analysis. A Retch AS 200 sieving machine analysed
the coarser grain fraction (4 mm—0.063 mm, wet sieving),
whereas a Cilas 1064 laser diffraction granulometer was used
for the finer one (0.0004—0.063 mm). Ultrasonic dispersion,
distilled water and sodium polyphosphate were used prior to
analyses in order to avoid a flocculation of particles. The
graphic mean (Mz) and inclusive standard deviation (
σI) were
used to demonstrate the average grain size and sediment sort-
ing (Folk & Ward 1957).
Fig. 1. Schematic map of the area under study with the location of
the monitoring sites.
149
PROVENANCE AND POLLUTANT TRACING OF FLUVIAL SEDIMENTS (MORAVIA, CZECH REPUBLIC)
Fig. 2.
Simplified
geological
map
and
stratigraphic
chart
of
the
area
under
study
–
according
to
Novák
(Ed.)
(1994),
Pesl
(Ed.)
(1982),
and
Müller
(2001).
150
NEHYBA, ADAMOVÁ, FAIMON, KUCHOVSKÝ, HOLOUBEK and ZEMAN
The gravel mineral composition (the
grains > 2 mm in diameter) was studied
under a binocular microscope. Geochemi-
cal methods were used for the bulk-rock
composition of a finer fraction. Dry sedi-
ments were homogenized, ground with a
pestle and mortar and sieved using a 2 mm
sieve. The sample was melted with a lithi-
um tetraborate/metaborate mixture (Spec-
tromelt A12, Merck) and dissolved in
diluted nitric acid. The main oxide compo-
nents of silicate matrix (Li
2
O, Na
2
O, K
2
O,
MgO, CaO, Fe
2
O
3
, TiO
2
, Al
2
O
3
, SiO
2
,
P
2
O
5
and SO
3
) were determined by ICP-
OES (Jobin-Yvon 170 Ultrace, JY-Horiba,
France). The total heavy metal content
(As, Cd, Co, Cr, Cu, Mo, Ni, Pb, Sb, V,
Zn) was determined by sample dissolution
and by analysing the solution obtained.
The ISO 14869-1 procedure was used for
the silicate matrix decomposition in an
open vessel system by a mixture of hy-
drofluoric and perchloric acid. 1 g of the
pulverized sample was used for the disso-
lution and the sample solution was dilut-
ed adequately prior to analysis. ICP—MS
(Agilent 7500ce, Agilent Technologies,
Japan) was used for the determination of
heavy metals. The elements suffering
from polyatomic interferences were mea-
sured in a He collision mode using the
Octopole Reaction System. Internal stan-
dards (Ge, In, Bi) were applied in order to
eliminate the matrix effect. The total con-
Fig. 3. Fluvial discharge for Dřevnice and Lutonínka Rivers in the years 2005 and 2006.
Arrows show sampling events in spring and autumn 2005 and 2006, respectively.
(apatite), the value of CaO is consequently accepted if the
mole fraction of CaO
≤Na
2
O. However, if CaO
≥Na
2
O, then it
was assumed that the moles of CaO=Na
2
O (McLennan 1993;
Bock et al. 2008). The Vsetín, Újezd, Ráztoka, and Lukov
Flysch Sandstones are denoted as VFS, UFS, RFS, and LFS, re-
spectively. The Vsetín, Újezd, Ráztoka, Lukov, and Belověž
Flysch Mudstones are denoted as VFM, UFM, RFM, LFM, and
BFM, respectively. Quaternary Loesses are denoted as QL.
Results
Grain size
The distribution of the individual particle size classes of the
studied samples is presented in Table 1. Sand and silt predom-
inate in the majority of the studied samples. Based on Folk
(1968), the sediments were classified as sands (33.3 %), silty
sands (27.8 %) or sandy silts (22.2 %). Sandy gravels
(11.1 %) and silts (5 %) are less frequent. The gravel content
is mostly negligible apart from some SS (typically 3). The
content of clay fraction is relatively low and slightly rises
downstream. The graphic mean varies between —1.5 and 6.3
φ,
but mostly between 2.8 and 4.9
φ (72.2 %). The σI values var-
ied between 1.3 and 3.5
φ, which indicates poor to extremely
tent of mercury was determined by the thermooxidation meth-
od using an AMA-254 analyser (Altec, Czech Republic). The
accuracy of the methodology was verified by an analysis of
the soil certified reference materials (ANA 7001—7004, Ana-
lytika Prague, Czech Republic).
The mineralogy of the clay fraction of modern deposits was
evaluated by RTG diffraction at Stoe Stadi P. diffractometer.
Measurement conditions: Co-K
α
1
radiation (1.78896
A
), ac-
celerating voltage 40 kV, beam 30 mA, reflection mode, lin-
ear PSD detector, step in 0.01 2
Θ, counting time of 3 s. Low
content of clay fraction in the studied sediment led to RTG
quantitative phase analyses.
The source rock samples were analysed in the laboratories
of the Czech Geological Survey Prague. The complete silicate
analysis (oxides of major elements and certain minor ele-
ments) and a standard set of trace elements were determined
by X-ray fluorescence (fm. Philips PW1410) and emission
spectral analysis (spectrograph fm. Zeiss). The mineral com-
position was determined by X-ray diffraction analysis (com-
plemented by automatic diffraction phase analyses); the
results were compared with those obtained by a differential
thermal analysis. Due to the highly varying carbonate content
and absence of CO
2
data, a precise correction for the carbonate
CaO was difficult for the chemical index of alternation (CIA
index – Young & Nesbitt 1998). After correcting for P
2
O
5
Å
151
PROVENANCE AND POLLUTANT TRACING OF FLUVIAL SEDIMENTS (MORAVIA, CZECH REPUBLIC)
Fig. 4. Areal distribution of the graphic mean (Mz) for the deposits in the studied moni-
toring sites. The values are in
Φ units.
Gravel (%)
Sand (%)
Silt (%)
Clay (%)
Mud (%)
Mz (
Φ) (σI)
Site code
Median (Minimum–Maximum)
SS 1
4.3 (3.6–7.4)
59.2 (55.5–70.1)
30.9 (20.2–31.9)
5.6 (4.0–7.5)
35.8 (25.5–39.4)
3.4 (3.0–4.1)
2.6 (2.4–2.8)
SS 2
1.4 (0.1–4.5)
69.7 (39.8–72.6)
23.1 (18.5–52.0)
5.9 (4.4–7.9)
29.0 (22.9–59.8)
3.2 (2.8–4.8)
2.4 (2.0–3.4)
SS 3
19.4 (4.2–30.4)
71.8 (64.6–85.1) 7.3 (4.1–8.6)
1.5 (0.9–2.1)
8.8 (5.0–10.7)
1.0 (0.0–1.7)
2.0 (1.3–2.2)
SS 4
3.1 (1.1–3.9)
61.4 (43.9–74.2)
30.3 (18.6–48.4)
5.0 (3.8–6.6)
35.3 (22.4–55.0)
3.4 (2.9–4.3)
2.4 (2.3–2.7)
SS 5
10.1 (0.1–49.8)
67.4 (39.9–75.7)
18.0 (8.3–22.5)
3.4 (1.6–4.0)
21.8 (9.9–25.7)
2.6 (–0.1–3.3)
2.4 (1.9–3.4)
SS 6
1.4 (0.4–2.4)
68.6 (62.3–72.2)
23.5 (18.6–32.9)
3.4 (3.3–4.4)
26.8 (22.1–37.3)
3.4 (3.2–3.8)
2.2 (2.0–2.3)
SS 7
1.0 (0.5–1.5)
48.2 (32.2–59.7)
45.6 (35.7–60.2)
4.7 (4.0–7.1)
50.4 (39.7–67.3)
4.3 (3.8–4.9)
2.0 (1.9–2.1)
SS 8
0.2 (0.0–0.8)
23.6 (13.3–40.9)
66.3 (50.9–72.6) 8.7 (6.9–16.9)
76.2 (58.3–86.7)
5.3 (4.6–6.3)
1.9 (1.8–2.2)
SS 9
9.4 (1.2–62.2)
38.1 (31.7–64.0) 36.4 (5.6–47.5)
4.9 (0.6–9.8)
41.4 (6.1–57.3)
3.4 (–1.5–3.9)
2.5 (2.1–3.5)
Table 1: Characteristics of sites – grain-size characteristics of the studied modern fluvial deposits.
poor sorting. The samples with a higher value of Mz are gen-
erally better sorted than the samples with a lower value. The
grain size of samples from the spring and autumn seasons are
usually similar with respect to individual SS. The along
stream variation is better developed in the spring samples
when slightly finer grained spring sediments were recognized
in most upstream SS and coarser grained deposits in most
downstream SS. The downstream fining of the studied depos-
its can be accepted when taking into account the confluences
(Fig. 4). Additional/transverse sources of material (bank ero-
sion, transport from the adjacent slopes or ravines) to the main
axial fluvial drainage are supposed close to the monitoring
sites 3, 9. Deposits of Holocene alluvial fans were recognized
adjacent to these monitoring sites. Additional provenance
from these deposits and so an important role of local sources is
supposed. Torrential water from the summer storms can trans-
port the coarser material from adjacent slopes to the river
course and accentuate the additional/transverse source of sedi-
ment at selected localities.
Gravel petrography
Three different types of material were recognized: (i) an-
thropogenic material (fragments of glass, bricks, concrete, as-
phalt, plastics), (ii) organic material (plant detritus, seeds), and
(iii) rock debris (predominantly sandstones, conglomerates,
quartzes, limestones, mudstones, exceptionally gneisses or
granitoids). The content of these materials differs both areally
and seasonally (Fig. 5). The organic material completely pre-
dominates in certain SS (typically 1, 6, 7, 8) and is usually
more common during the autumn. A higher content of anthro-
pogenic material is typical for downstream samples (usually
SS 6—9) and its content seems to be enhanced in the spring.
An absolute dominance of rock debris can usually be observed
in SS 3 and 5, whereas it is absent or very low downstream
(particularly SS 6—8). The content of the organic material is
generally higher in finer-grained fraction, whereas a coarser
content typically reveals a higher presence of rock debris and
anthropogenic material (Fig. 6A,B,C).
Clay mineralogy
Significant differences in mineralogy existed between the re-
sults from individual monitoring sites from the single sampling
season and also different seasons. Semiquantitative evaluation
of all studied samples is presented in the Table 2. Individual
minerals were evaluated by numbers to reflect their relative oc-
currences (0 – not present, 1 – very rare, 2 – rare, 3 – medi-
um, 4 – abundant, 5 – very abundant).
Quartz is the most abundant mineral. Content of illite and
kaolinite is relative stable. Significant variations can be fol-
lowed in the role of smectite. Significant differences can also
be followed for the content of chlorite. The content of feldspar
also varies. Presence of feldspar is in general relatively lower
in the autumn samples (compared with the
spring ones). Presence of plagioclase is
usually more important than the presence
of feldspar (Dosbaba 2008).
Major elements
The major elements for the sediments
are given in Table 3. The SiO
2
content
ranges widely from 60.7 to 83.7 wt. %
and is consistent with site lithologies
(Fig. 7A). The main element content re-
veals both areal and seasonal variations
with an inverse dependence on grain size
(particularly for K
2
O, Na
2
O, MgO, Al
2
O
3
,
Fe
2
O
3
, and
TiO
2
– Fig. 7B—D). The grain
size effect on chemical composition sug-
gests
SiO
2
/Al
2
O
3
—Na
2
O/K
2
O
diagram
(Fig. 7E) (see Ohta 2008).
152
NEHYBA, ADAMOVÁ, FAIMON, KUCHOVSKÝ, HOLOUBEK and ZEMAN
The positive inter-relationship amongst Al
2
O
3
and
TiO
2
is
well developed (Fig. 8A). A diagram of Al
2
O
3
vs. TiO
2
and
the Ti : Al ratio were used for studies of the provenance and
weathering extent (Young & Nesbitt 1998). The Ti : Al ratio
for the studied samples varies between 0.12 to 0.17 and is
generally higher downstream. A negative correlation be-
tween TiO
2
and SiO
2
is generally supposed (Fig. 8B). K
2
O/
Al
2
O
3
ratio is between 0.17—0.29 and its relation to grain
size is complex (Fig. 8C). The coarser samples (Mz below
3
φ) and the finer ones (Mz above 3 φ) seem to form two
subpopulations in the diagram.
The deposits can be classified as lithic arenites, apart from
several which are sublithic arenites and wacke (see Fig. 8D
according to Herron 1988). The content of total alkali is rela-
tively low. Alongstream, irregular variations in the content
of the major elements are developed (Fig. 8E—H). A decline
in the SiO
2
content can usually be observed between the
SS 3—4 and 6—8 and an increase at SS 3, 5 and 8. The oppo-
site trend, namely a rise between the SS 3—4 and 6—8 and a
decline at SS 3 and 9 can often be seen in the content of
K
2
O, Na
2
O, CaO, MgO, Al
2
O
3
, TiO
2
and Fe
2
O
3
. These
trends are slightly obliterated by seasonal variations. The up-
stream sediments could be slightly higher with an abundance
of K
2
O, Na
2
O, CaO, MgO, Al
2
O
3
, TiO
2
and
Fe
2
O
3
,
and low-
er in SiO
2
. An inverse relation between the grain size and the
Ti : Al ratio can be observed (Fig. 9).
Fig. 5. Composition of the gravelly grain size fraction (2—8 mm) of
the studied sediments.
Fig. 6. Relations of the graphic mean Mz and: A – the content of
anthropogenic material in gravel fraction, B – the content of or-
ganic material in gravel fraction, C – the content of rock debris in
gravel fraction.
Table 2: Semiquantitative mineralogy of the clay fraction of the
studied sediments.
Mineral
Spring 2005 Autumn 2005 Spring 2006 Autumn 2006
Smectite
3.3 4.3 2.1 2.4
Chlorite
1.7 1.3 2.2 1.4
Illite
4.0 3.5 3.9 3.7
Kaolinite
3.0 3.2 2.8 2.9
Quartz
5.0 4.7 5.0 5.0
Feldspar
2.3 1.2 2.1 1.4
Plagioclase
2.0 1.8 3.0 2.6
Provenance
The chemical composition of clastic sediments is a result of
a number of geological factors (source rock composition,
chemical weathering intensity, sediment supply rate, and tex-
tural/mineralogical/hydraulic sorting) (Johnsson 1993; Cox &
Lowe 1995; Sensarma et al. 2008).
The value of the ratio K
2
O/Na
2
O (Roser & Korsch 1986)
for the studied sediments varies between 2.55 and 4.71. This
153
PROVENANCE AND POLLUTANT TRACING OF FLUVIAL SEDIMENTS (MORAVIA, CZECH REPUBLIC)
Fig. 7. Relation between the graphic mean (Mz) and A – the con-
tent of SiO
2
, B – the content of TiO
2
and MgO, C – the content of
Al
2
O
3
and Fe
2
O
3
, D – the content of K
2
O and Na
2
O, E – plots of
the SiO
2
/Al
2
O
3
—Na
2
O/K
2
O diagram reflecting the effect of hydrau-
lic sorting. Sediments derived from a recycled sedimentary prove-
nance delineate horizontal trends (see Ohta 2008).
high value reflects a derivation from the recycled sedimentary
sources (McLennan et al. 1993; Bock et al. 1998).
A multivariate cluster analysis (Ward’s method as an algo-
rithm) was applied to compare the chemical composition of the
source rocks and the sediments (Fig. 10). Ten major/minor ele-
ments (Si, Ti, Al, Fe, Mn, Mg, Ca, Na, K, P) and seven trace el-
ements (Cr, Cu, Ni, Pb, Zn, V, Co) were considered. Based on
the analysis, the samples were clustered into two principal
groups. The first one (see the group on the left side in Fig. 10)
linked 12 sediments to the source flysch mudstones (RFM,
BFM, LFM, VFM, UFM). The second group linked the remain-
ing 24 sediment samples to the source flysch sandstones (VFS,
UFS, RFS, LFS). Of these 24 samples, 11 sediments were more
tightly associated with the source Quaternary loeses (QL), see
the subgroup separated from the second group on the right side
of Fig. 10. In the single groups, the sediments of all the seasons
were mixed (Table 4). The chemical compositions of the poten-
tial source rocks are presented in Table 5a,b.
With respect to the SS, the sediments of the first group with
the source mudstones were particularly dominant downstream
(particularly on SS 7 and 8). The sediments with the source
sandstones mainly predominate upstream (SS 1, 2 and also 5).
The loesses source is typical for the middle part of the area
(SS 3, 6, 4).
The studied sediments were plotted onto the Al
2
O
3
—
(CaO + Na
2
O)—K
2
O diagram (Fig. 11A), the A—CN—K in the
154
NEHYBA, ADAMOVÁ, FAIMON, KUCHOVSKÝ, HOLOUBEK and ZEMAN
next text, and the CIA index was calculated. The weathering
indices reflect in this case a variation in possible parent rock
composition rather than the degree of weathering (Borghes &
Huh 2007). The samples follow a trend of increasing Al
2
O
3
and K
2
O with decreasing CaO + Na
2
O. The CIA index ranges
between 54 and 74, with the majority of samples ranging be-
tween 64 and 73. The annual CIA variations are larger than
the areal ones, although the downstream samples show a
slightly higher CIA index.
The possible source rocks were plotted in the A—CN—K dia-
gram (Fig. 11B). The similar pattern can be followed in both
modern and possible source rocks, that is, the contents of Al
2
O
3
and K
2
O increase when CaO + Na
2
O decreases. The CIA index
for the flysch sandstones varies between 61 and 68, and for the
flysch mudstones between 71 and 80. Neogene clays and Qua-
ternary loesses show mean values in the CIA index of about 83
and 74, respectively. The Ti : Al ratio for the flysch sandstones
varies between 0.07 and 0.15, and for the flysch mudstones be-
tween 0.10 and 0.12. Neogene clays have an average value of
the CIA of about 0.11 and Quaternary loesses of about 0.16.
Trace elements/heavy metals
The heavy metal contents in the studied samples are given
in Table 6. They vary highly, both areally and seasonally.
High seasonal variations were recognized in particular for Pb
and V. The contents of Pb, Ni, V, Cr, Cd, Zn, Cu, and Sb are
influenced by lithology (Fig. 12A—E), the finer grained sam-
ples usually reveal a higher content of the metals. However, a
lack of a simple linear pattern (particularly for Pb, Zn, Cd and
Sb) also indicates further factors influencing the content of
these elements.
Alongstream irregular variations in the content of heavy
metals are visible (Fig. 13A—E) similarly to major elements.
The highest concentrations were usually most apparent down-
stream (SS 7 and 8), with the exception of Ni, and Pb. The
samples from the furthest upstream SS 1 and 2 often revealed
enhanced concentrations of metals (particularly Ni). The con-
tent of all the heavy metals decreased at SS 3 and increased
(often rapidly) at SS 7. A downstream increase in the content
of Ni, Cr and V was recognized between SS 3—4 and 7—8. The
opposite trend, namely a decrease between the same SS, was
recognized for Sb, Zn, Pb and Cd.
The content of the heavy metals in potential source rocks is
demonstrated in Table 5B. Flysch sandstones contain remark-
ably lower contents of heavy metals than their mudstone
“counterparts” as well as in comparison with Quaternary
Table 3:
Characteristics of sites – sediment major element composition.
mudstone
group
sandstone-
loess group
sandstone
subgroup
loess
subgroup
spring
5 13 7 5
autumn
7 11 5 6
2005
5 13 5 7
2006
7 11 7 4
sampling point
mean number
7
4
3.6
4.7
Table 4: Results of cluster analysis: Numbers of individual sedi-
ment samples in single groups of sources rocks in single seasons
and mean position of sampling point.
Si
te
cod
e
Al
2
O
3
(%
)
Ca
O (%
)
Fe
2
O
3
(%
)
K
2
O (%
)
L
iO
2
(%
)
Mg
O (%
)
MnO (%
)
Na
2
O (%
)
T
iO
2
(%
)
P
2
O
5
(%
)
Si
O
2
(%
)
Me
di
an
(
M
ax
im
um
–M
in
im
um
)
SS 1
7.
81
(
6.71–
8.3
1)
3.
72
(
4.08–
3.
23
)
3.
73
(
4.25–3.
23
)
1.
50
(
1.68–
1.
41
)
0.
01
(
0.02–
0.
01
)
1.
19
(
1.27–
1.
00
)
0.
17
(
0.20–
0.
11
)
0.
47
(
0.61–
0.
35
)
0.
50
(
0.54–
0.
40)
0.
14
(
0.18–
0.
10
)
70
.6
7 (
74.8
8–66
.5
6)
SS 2
7.
55
(
9.14–
6.6
1)
6.
86
(
7.75–
6.
30
)
4.
00
(
4.45–3.
43
)
1.
43
(
1.66–
1.
21
)
0.
01
(
0.02–
0.
01
)
1.
11
(
1.37–
0.
97
)
0.
12
(
0.17–
0.
09
)
0.
49
(
0.61–
0.
37
)
0.
48
(
0.62–
0.
41)
0.
15
(
0.20–
0.
11
)
66
.9
3 (
70.7
0–60
.7
0)
SS 3
4.
38
(
4.62–
4.0
6)
4.
10
(
4.91–
3.
25
)
2.
52
(
4.91–3.
25
)
0.
93
(
1.11–
0.
85
)
0.
01
(
0.01–
0.
01
)
0.
62
(
0.68–
0.
55
)
0.
09
(
0.09–
0.
08
)
0.
33
(
0.43–
0.
23
)
0.
27
(
0.28–
0.
25)
0.
09
(
0.11–
0.
05
)
81
.1
9 (
82.5
3–79
.7
1)
SS 4
6.
04
(
8.89–
4.3
4)
3.
28
(
4.11–
2.
62
)
2.
99
(
4.1
1–2.
62
)
1.
21
(
1.60–
0.
86
)
0.
02
(
0.02–
0.
01
)
0.
84
(
1.31–
0.
57
)
0.
11
(
0.12–
0.
08
)
0.
39
(
55
.5–
70
.1
)
0.
42
(
0.59–
0.
30)
0.
15
(
0.27–
0.
08
)
76
.6
2 (
83.7
0–65
.2
9)
SS 5
6.
54
(
6.71–
6.4
0)
2.
03
(
2.89–
1.
37
)
2.
82
(
2.89
–
1.37
)
1.
61
(
1.91–
1.
38
)
0.
01
(
0.02–
0.
01
)
0.
71
(
0.75–
0.
67
)
0.
09
(
0.13–
0.
05
)
0.
69
(
0.46–
0.
30
)
0.
42
(
0.43–
0.
39)
0.
09
(
0.11–
0.
08
)
79
.8
4 (
82.2
5–77
.3
7)
SS 6
5.
72
(
7.09–
5.0
1)
2.
83
(
3.34
–2
.11
)
2.
54
(
3.34–2.
11
)
1.
29
(
1.44–
1.
02
)
0.
01
(
0.02–
0.
01
)
0.
69
(
0.91–
0.
56
)
0.
09
(
0.11–
0.
06
)
0.
39
(
0.64–
0.
36
)
0.
38
(
0.45–
0.
39)
0.
16
(
0.29–
0.
06
)
78
.8
9 (
83.4
7–74
.1
2)
SS 7
7.
71
(
8.87–
7.2
0)
4.
90
(
5.58–
4.
60
)
2.
90
(
5.58–4.
60
)
1.
56
(
1.78–
1.
34
)
0.
01
(
0.02–
0.
01
)
0.
99
(
1.14–
0.
90
)
0.
09
(
0.12–
0.
06
)
0.
49
(
0.48–
0.
29
)
0.
54
(
0.63–
0.
5)
0.
24
(
0.28–
0.
22
)
67
.5
6 (
69.2
9–65
.3
6)
SS 8
10
.26
(
12
.29
–8.
06
)
3.
06
(
3.65–
2.
58
)
4.
14
(
3.65–2.
58
)
2.
01
(
2.37–
1.
5)
0.
01
(
0.03–
0.
01
)
1.
21
(
1.44–
0.
92
)
0.
12
(
0.14
–0
.09
)
0.
60
(
0.66–
0.
46
)
0.
72
(
0.84–
0.
60)
0.
29
(
0.36–
0.
22
)
67
.2
8 (
74.2
7–62
.0
6)
SS 9
8.
21
(
9.60–
6.0
1)
3.
01
(
3.36–
2.
80
)
3.
28
(
3.36–2.
80
)
1.
64
(
1.72–
1.
53
)
0.
01
(
0.02–
0.
01
)
0.
96
(
1.13–
0.
69
)
0.
12
(
0.14–
0.
09
)
0.
57
(
0.63–
0.
47
)
0.
53
(
0.67–
0.
37)
0.
28
(
0.39–
0.
20
)
73
.7
4 (
78.3
4–68
.8
7)
155
PROVENANCE AND POLLUTANT TRACING OF FLUVIAL SEDIMENTS (MORAVIA, CZECH REPUBLIC)
Fig. 8. Relation between: A – the content of TiO
2
and
Al
2
O
3
, B – the content of SiO
2
and TiO
2
, C – K
2
O/Al
2
O
3
and the graphic mean (Mz),
D – Compositional maturity of studied sediments (Herron 1988). The alongstream distribution of major oxides: E – Si
2
O, F – Al
2
O
3
,
G – Na
2
O, H – K
2
O.
156
NEHYBA, ADAMOVÁ, FAIMON, KUCHOVSKÝ, HOLOUBEK and ZEMAN
loesses. A comparison of sediments and their possible prove-
nance rocks with respect to the content of heavy metals is pre-
sented in Fig. 14.
Relatively immobile trace elements, Cr and, Ni, are general-
ly believed to undergo the least fractionation during sedimen-
tary processes (Hassler & Lowe 2006). The Cr/Ni ratio of the
studied samples varies between 1.03 and 2.09 (1.37 on aver-
age). In comparison with the source rocks, the ratio was less
than for flysch sandstones (2.2—3.4), partly for flysch mud-
stones (1.6—3.9) and Quaternary loesses (1.9 on average).
Fig. 9. Relations of the graphic mean (Mz) and Ti/Al.
Fig. 10. Multivariate data cluster analysis based on chemical composition of sediments and source rocks (Vard’s method). The source rocks are
highlighted (Vsetín, Újezd, Ráztoka, and Lukov Flysch Sandstones are denoted as VFS, UFS, RFS, and LFS. Vsetín, Újezd, Ráztoka, Lukov,
and Belověž Flysch Mudstones are denoted as VFM, UFM, RFM, LFM, and BFM. Quaternary Loesses are denoted as QL. Modern sediment
samples are denoted as A or S: autumn or spring season, 05 or 06: 2005 or 2006 year of sampling, and 1—9: number of sampling site).
Fig. 11. Ternary plot CN—A—K for: A – studied sediment and B – source rocks.
157
PROVENANCE AND POLLUTANT TRACING OF FLUVIAL SEDIMENTS (MORAVIA, CZECH REPUBLIC)
Table 5: The chemical composition of potential source rocks: A – major elements (results in %), B – heavy metals (results in ppm).
Interpretations and discussion
A combination of grain size, petrography and geochemis-
try enable an evaluation of source rocks and the factors con-
trolling sediment composition. The data on modern fluvial
deposits revealed that their mineralogy and chemistry
changed with grain size. It is due to (1) multiple sources con-
tributing to grains with mineralogically and texturally dis-
tinct characteristics, (2) physical weathering of non-stable
grains, and (3) sorting of compositionally distinct grains dur-
ing transport (Johnsson 1993). All these factors can be ob-
served in this study.
The prevalence of sand/silt and varied gravel role reflect a
wider spectra of transportation with a dominance of the sus-
pended load (Owens et al. 2005). A low presence of clay mainly
favours transport as discrete particles (Dropo & Ongley 1994).
Although the longitudinal transport of material dominates
within the fluvial basin, the role of confluences and addition-
al/transverse sources of material (bank erosion, adjacent
slopes or ravines) to the main axial drainage are locally im-
portant. The granules and pebbles formed by rock debris
mostly originated from the flysch rocks of the Rača Unit or
older fluvial and proluvial gravels. The anthropogenic and
organic materials in the gravel fraction are linked to human
activities. Seasonal differences in their relative content can
be due to the following: i) the annual cycle of the harvest
season and plant production with its peak in the summer
months and/or, ii) a different mode of erosion and prove-
nance reflecting seasonal variability in fluvial discharge. The
higher downstream content of the coarse anthropogenic ma-
terial is associated with the position within densely populat-
ed urban areas (the towns of Zlín and Otrokovice). Human
activities are directly (anthropogenic material) or indirectly
(organic material) responsible for its delivery.
The seasonal variability in fluvial discharge plays an im-
portant role. Limited precipitation during the summer
months with torrential storms supports the erosion of coarser
A
B
Rocks
No. of analyses
SIO
2
TiO
2
Al
2
O
3
Fe
2
O
3
FeO MnO MgO CaO Na
2
O K
2
O P
2
O
5
VFS
22 80.7
0.3
4.4
1.4
0.7
0.04
0.7
2.1
0.6
0.9
0.06
UFS
2
83.1
0.21
4.0
0.7
0.13
0.09
0.2
2.0
0.3
1.8
0.02
RFS
17 82.0
0.3
6.9
0.8
1.4
0.04
0.7
1.9
1.0
1.8
0.04
LFS
9
85.6
0.22
6.7
0.6
0.3
0.02
0.2
0.3
0.8
2.4
0.02
VFM
47
51.4 0.62 12.3 3.5 0.9 0.08 1.7 10.4 0.4 2.6
0.08
UFM
19
56.8
0.86
16.8
5.1
1.0
0.12
2.7
1.9
0.9
3.1
0.12
RFM
23
56.6
0.97
19.8
4.1
1.7
0.03
2.3
0.6
0.8
4.5
0.09
LFM
4
55.9
1.01
21.9
3.9
1.0
0.03
1.7
0.5
0.4
4.9
0.07
BFM
26
55.4 0.87 19.2 7.3 1.0 0.08 2.1
0.5 0.5 3.7 0.1
QL
6
70.4
0.79
11.3
3.5
0.4
0.07
1.1
2.2
0.9
2.2
0.23
Rocks
No. of analyses
As
Be
Cr
Cu
Mo
Ni
Pb
Zn
V
Co
VFS
22
<5
1
65
9
1
19
6
20
34
5
UFS
2
<5
1
34
5
1
16.5 10.5 8
13.5 5
RFS
17
<5
1
28
7
1
12
12
28
26
5
LFS
9
<5
2
20
8
<1
9
18
16
15
<5
VFM
47
<5
2.1 107
42
<1
56
16
85
112
13
UFM
19
5
2
266
57
<1
161
22
124
158
26
RFM
23
5
4
138
52
1
55
30
109
153
16
LFM
4
5
4
116
51
1
30
30
82
155
11
BFM
26
<5
4
139
68
<1
86
31
124
141
23
QL
6
7.8 1.6 68.0 17.2
<7
35.5 10.2 56.7 57
11.3
detritus from adjacent slopes to the river course particularly
upstream and also accentuates the role of local sources. More
regular and higher fluvial discharge during the late autumn,
winter and spring favours a wider/variegated provenance
and a downstream redeposition of the material within the flu-
vial course. The progressive reduction of grain size, even
subtle, and increasingly better sorting of sediment within a
reasonably short transport distance ( > 70 km) could indicate
the role of either the weathering processes in the catchment
area (Sensarma et al. 2008) or the recycling/select redistribu-
tion of the material.
The studied deposits are relatively immature. The linear and
almost horizontal arrangement of the data in Fig. 7E and the
low K
2
O/Al
2
O
3
ratios indicate a recycling of the source
quartz-rich sedimentary rocks (Cox & Lowe 1995; Passchier
2004), a similar source and a relatively low content of phyllo-
silicates as well as the important role of quartz.
With no extra input of detritus, the sediment recycling re-
sults in a negative correlation between SiO
2
and TiO
2
(Gu et
al. 2002) and its product will contain more quartz (i.e. SiO
2
),
less feldspar and clays (lower content of TiO
2
, Al
2
O
3
and
MgO) (Cox & Lowe 1995; Corcoran 2005). Although the
role of recycling in the studied deposits can be documented
in general, SiO
2
and TiO
2
do not show a consistent negative
correlation. It points to a situation when simple alongstream
recycling is “complicated” by an additional transverse input
of the “fresh” material into the fluvial course. The relative
preferential removal of finer-grained material in the up-
stream part of the basin with its enrichment downstream also
influenced the composition.
The different relation of grain size with SiO
2
vs. K
2
O,
Na
2
O, MgO, Al
2
O
3
, Fe
2
O
3
, and
TiO
2
reflects variations in
the mineral composition (quartz vs. feldspar, plagioclases,
clay minerals) in different grain size fractions. The low con-
centration of alkali elements and their negative correlation to
SiO
2
reflects the relatively low presence of feldspar and pla-
gioclases, and the dominance of quartz. Areal variations in the
158
NEHYBA, ADAMOVÁ, FAIMON, KUCHOVSKÝ, HOLOUBEK and ZEMAN
Fig. 12. Relation between the graphic mean (Mz) and: A – the con-
tent of Pb, B – the content of Ni and Cu, C – the content of V and
Cr, D – the content of Zn, E – the content of Cd and Sb.
content of major elements are not consistent with element rel-
ative mobility during weathering and reveals a relation be-
tween chemical composition and lithologies (similarly as
Passchier & Whitehead 2006). The increase in the abundance
of heavy metals and iron with decreasing grain size reflects
the higher concentration of certain minerals (pyroxene,
chromite, chlorite) in finer grain size fractions and, possibly, a
sorption of heavy metals on an organic substance.
The similarity of CIA values with possible source rocks
and tight clustering near the feldspar join in the triangular plot
A—CN—K (Fig. 11A,B) indicates mainly physical weathering
and the low role of chemical weathering. The elongated distri-
bution of the studied samples in the A—CN—K diagram reflects
the varied role of the weathering trend/clay minerals and can
be associated with grain size variations (Corcoran 2005). The
CIA values are typical of recycled sediments (Young & Nes-
bitt 1998) and its variations reflect differences in the propor-
tions of feldspar versus aluminous clay minerals. The effect of
chemical weathering depended on (1) intensity (controlled pri-
marily by the climate and vegetation) and (2) available time
159
PROVENANCE AND POLLUTANT TRACING OF FLUVIAL SEDIMENTS (MORAVIA, CZECH REPUBLIC)
Fig. 13. The alongstream distribution of A – the content of Pb, B –
the content of Ni and Cu, C – the content of V and Cr, D – the con-
tent of Cd and Sb, E – the content of Zn.
for weathering. The second effect including a complex set of
factors, the physiography of which is particularly important
(Johnsson 1993; Le Pera et al. 2001). A typical fractionation
(Cox & Lowe 1995) was not achieved because the mud frac-
tion of the studied sediments does not consist mainly of the
clay minerals formed by the chemical alteration of the source
rocks. Erosion on the relatively steep slopes tends to (1)
quickly isolate detritus from the weathered rocks and (2) rapid
and short transport leads to minimal sediment maturation and
alteration. Among the muds, quartz is enriched by more unsta-
ble phases, particularly by the breakdown of lithic fragments
and granular disintegration (Johnsson & Meade 1990). The re-
lief suggests mechanical erosion with rapid sediment transport
and short temporary storage. Chemical weathering during
transport appears to be negligible; it was suppressed by me-
chanical disintegration which is considered the main mecha-
nism responsible for sand compositional variation during
fluvial transport (Ibbeken & Schleyer 1991). Chemical alter-
ation and mechanical breakdown of the source rocks, followed
by hydraulic sorting of particles during transport, often leads
160
NEHYBA, ADAMOVÁ, FAIMON, KUCHOVSKÝ, HOLOUBEK and ZEMAN
Site
c
ode
A
s (ppm
)
C
d
(pp
m
)
C
o (
p
p
m
)
C
r (pp
m
)
C
u (pp
m
)
Hg
(pp
m
)
N
i (pp
m
)
P
b (pp
m
)
Sb (
p
pm
)
V
(pp
m
)
Z
n (
pp
m
)
M
ed
ia
n (M
inim
um
–M
ax
im
um
)
SS
1
6.
21 (
4.
80–7.
48)
0.
25 (
0.
19–0.
31)
17.
60
(
12.
70–
24.
70)
67.
10 (
57.
70–
79.
80)
29.
73 (
25.
53–31
.90)
0.
05 (
0.
04–0.
07)
60
.03 (
51.
90–71.
30)
33.
76
(
26.
10–60.
40)
0.
67 (
0.
45–1.
00)
63.
86 (
56.
00–7
2.
90)
106.
54 (
88.
54–
137.
0)
SS
2
6.
33 (
5.
20–6.
90)
0.
26 (
0.
20–0.
32)
15.
99
(
11.
90–
19.
60)
64.
58 (
51.
20–
85.
00)
38.
35 (
32.
50–50
.90)
0.
05 (
0.
04–0.
08)
55
.16 (
49.
60–60.
40)
35.
10
(
34.
30 – 37.
80)
1.
00 (
0.
60–1.
51)
64.
78 (
51.
10–7
6.
20)
133.
40 (
121.
0–
177.
0)
SS
3
4.
30 (
4.
00–4.
62)
0.
17 (
0.
13–0.
26)
9.
30
(
7.
80–
11.
54)
35.
07 (
31.
50–
42.
30)
28.
24 (
19.
51–41
.10)
0.
05 (
0.
04–0.
07)
30
.73 (
28.
40–32.
17)
35.
29
(
20.
70–61.
50)
0.
77 (
0.
56–1.
00)
33.
89 (
30.
10–3
7.
36)
92.
09 (
122.
08–
177.
0)
SS
4
4.
32 (
3.
819–4.
40
)
0.
26 (
0.
10–0.
40)
11
.18 (
9.
80–
12.
20)
48.
92 (
40.
56–
64.
20)
33.
82 (
17.
31–59
.10)
0.
09 (
0.
02–0.
09)
40
.47 (
33.
40–50.
40)
26.
44
(
20.
80–34.
40)
0.
80 (
0.
34–1.
50)
45.
93 (
36.
55–6
2.
10)
125.
35 (
74.
52–
106.
0)
SS
5
4.
89 (
4.
00–5.
30)
0.
22 (
0.
10–0.
32)
11.
06
(
6.
40 –
14.
99)
42.
24 (
31.
70–
48.
35)
22.
50 (
16.
80–24
.60)
0.
05 (
0.
04–0.
07)
32
.52 (
25.
20–38.
14)
30.
92
(
20.
90–37.
20)
0.
52 (
0.
20–0.
70)
47.
72 (
35.
80–5
4.
91)
114.
05 (
62.
0–
241.
0)
SS
6
3.
75 (
3.
34–4.
04)
0.
21 (
0.
16–0.
30)
10
.11 (
7.
80–
12.
66)
40.
79 (
38.
40–
44.
20)
26.
46 (
20.
04–37
.20)
0.
11 (
0.
05–0.
23)
32
.85 (
30.
60–35.
31)
22.
73
(
21.
66–24.
30)
0.
58 (
0.
41–0.
80)
40.
36 (
37.
50–4
3.
80)
109.
11 (
93.
5–
126.
79)
SS
7
4.
49 (
3.
40–4.
93)
0.
60 (
0.
54–0.
70)
12
.29 (
7.
60–
16.
70)
61.
00 (
46.
10–
79.
20)
51.
09 (
41.
12–66
.90)
0.
37 (
0.
26–0.
45)
40
.28 (
30.
50–48.
10)
32.
57
(
28.
10–41.
30)
1.
44 (
1.
11–1.
73)
58.
14 (
43.
30–6
9.
40)
214.
37 (
175.
66–
274.
0)
SS
8
6.
97 (
5.
45–9.
60)
0.
55 (
0.
44–0.
70)
14.
12
(
10.
60–
18.
56)
81.
54 (
70.
50–
96.
20)
44.
61 (
40.
50–50
.54)
0.
31 (
0.
19–0.
47)
44
.68 (
38.
00–36.
48)
32.
22
(
28.
20–34.
68)
1.
29 (
1.
06–1.
60)
77.
15 (
59.
50–9
5.
80)
193.
87 (
180.
0–
213.
38)
SS
9
4.
88 (
3.
30–7.
00)
0.
49 (
0.
10–0.
61)
11
.02 (
9.
10–
12.
27)
58.
11 (
47.
20–
76.
20)
35.
05 (
25.
20–45
.40)
0.
28 (
0.
09–0.
46)
31
.94 (
30.
20–39.
10)
26.
87
(
13.
80–35.
60)
1.
00 (
0.
64–1.
50)
56.
04 (
46.
07–6
9.
50)
171.
79 (
81.
3–
242.
0)
to preferential enrichment of specific minerals in certain grain-
size fractions. Therefore, sediment composition tends to be a
function of grain size (Whitmore et al. 2004). A number of au-
thors have indicated that sediment grain size affects both mod-
al composition and geochemistry (Roser & Korsch 1986; Cox
& Lowe 1996; Whitmore et al. 2004).
The elongated line for the studied samples (Figs. 8a, 9) indi-
cates a mixing of sand with mud during deposition (see
Young & Nesbitt 1998) and is consistent with the composition
of flysch rocks (particularly sandstones) and Quaternary loess-
es. The reduction of Al content in comparison with possible
source rocks can be a result of preferential removal of Al in
the form of fine clay particles. The position of flysch mud-
stones does not completely fit with the linear array, being en-
riched both in Ti and mainly Al. The trends in Figs. 8a, 9 and
11a,b point to a non-uniform source. More coarse-grained
(sandy) samples show a lower content of both Ti and Al. In-
creased Al content in muds could be due to a separation of
fine-grained clay minerals from quartz and feldspar during
transportation. The behaviour of Ti could be explained by ei-
ther fine-grained Ti-rich minerals (Fe and Ti oxides or hydrox-
ides), by incorporation of Ti to clays, or by the partially
different provenance of the varied grain size fractions (Young
& Nesbitt 1998; Passchier & Whitehead 2006). Sandy grains
predominantly originate from flysch sandstones. The sand-
stones of the Vsetín Member are typical with a lower content
of Al and alkali elements and a high SiO
2
content. Loesses
have a high content of quartz (45—50 %), plagioclases form
about 11—14 % and mica minerals predominate in the clay
fraction (Adamová 1990a,b). The provenance from Quaterna-
ry loesses in the middle part of the area under study suits well
with their predominant occurrence in this area (see Fig. 2) and
the local source of material.
The alongstream variations in the heavy metal content re-
flect differences in the sediment provenance, but are also in-
fluenced by anthropogenic sources. In the upstream part of the
area (typically SS 1 and 2) a provenance from flysch sand-
stones predominates. The highly enhanced metal concentra-
tions in the deposits with respect to the source rocks are
ascribed to anthropogenic sources or, partially, originate from
flysch mudstones. The highest concentrations of metals were
in contrast recognized in the downstream area (particularly
Fig. 14. The content of selected heavy metals in both studied mod-
ern deposits and source rocks.
Table 6:
Characteristics of sites – sediment heavy mineral content (resu
lts in ppm).
161
PROVENANCE AND POLLUTANT TRACING OF FLUVIAL SEDIMENTS (MORAVIA, CZECH REPUBLIC)
SS 7 and 8), where the provenance from flysch mudstones
predominates. These mudstones are characterized by a high
concentration of metals. The concentrations of metals in the
modern sediments in these areas are usually lower than in the
source rocks, except for Pb and Zn. The lowest concentrations
of heavy metals were usually observed in the middle part of
the study area (SS 3, 4 and 6) which is typical for an important
source from the Quaternary loesses.
An enhanced abundance of ferromagnesian elements (Fe,
Mg, Mn, Cr, Ni, V, and Cr/Ni ratio) in sedimentary rocks is
usually interpreted as an indication of the provenance from
mafic and ultramafic igneous rocks (Bock et al. 2008). In this
study, the reason for the increased content of these metals is
ascribed to flysch mudstone source and anthropogenic pollu-
tion. The contents of Cr, Co, Cu, Ni, and V are affected only
locally or seasonally; their concentrations are usually similar
in modern sediments and source rocks.
The contents of Pb and Zn are highly enhanced in compari-
son with the natural background in the entire study area. The
anthropogenic source of Cr, Cd, Ni, Cu, As, Zn was demon-
strated in soils by comparing the studied area with soils
formed on similar parental rocks in adjacent areas (Adamová
1989). This situation reveals a complicated distribution of
metals in the adjacent modern depositional environments in
addition to different processes in their formation and prove-
nance. The rapid increase in heavy metal content is associated
with the urban area in the surroundings of the towns of Zlín
and Otrokovice. The rubber/shoe manufacturing industry and
traffic seem to be the main sources of pollutants.
The flysch deposits underwent the “separation” of sand-
stone and mudstone components during the weathering and
transportation processes. The sorting of grains with a distinct
grain size and composition led to the enrichment of the mate-
rial with the provenance from sandstone in the upstream area
whereas the material sourced from mudstones was enriched in
the downstream area. Several recycling/redeposition events
gradually influenced the reduction in the grain size. In addi-
tion, the grain size of sediments was controlled by the grain
size of the source rocks and by local sources, as the proportion
of sand-prone quartzes (SiO
2
) was reduced downstream.
Conclusions
The studied modern fluvial deposits from the Dřevnice Riv-
er Basin (eastern Moravia, Czech Republic) are relatively im-
mature; they are composed of predominantly lithic arenites,
apart from a few which are sublithic arenites and wacke. The
deposits are poorly sorted and can be predominantly classified
as sands, silty sands, or sandy silts. Both the gravel and clay
contents are relatively low.
Alongstream and seasonal variations in (1) grain size, (2)
gravel petrography, (3) clay mineralogy, and (4) geochemistry
(major elements, heavy metals) of modern sediments were
recognized. Differences in sediment fabric and composition
can be associated with a different mode of erosion, reflecting a
seasonal variability in fluvial discharge, and a different prove-
nance in various parts of the basin. More regular and higher
fluvial discharges during the late autumn, winter and spring
favour a larger/varied provenance and an alongstream sedi-
ment redistribution. In contrast, the limited precipitation dur-
ing the summer months supports the local erosion and local
provenance. The provenance study revealed the source of the
fluvial deposits from recycled older sedimentary rocks, more
precisely from flysch sandstones, flysch mudstones and Qua-
ternary loesses. The sediments with the source in flysch mud-
stones predominate far downstream, whereas the deposits with
the source in flysch sandstones predominate mainly upstream.
The ones with the provenance from loesses are typical of the
middle part of the studied area.
The contents of Pb and Zn are highly enhanced in compari-
son with the natural background in the study area. The rapid
increase in heavy metal content is associated with the urban
area in the surroundings of the towns of Zlín and Otrokovice.
The anthropogenic sources of Pb and Zn are connected with
the rubber/shoe manufacturing industry and traffic. The con-
tents of other heavy metals, namely Cr, Co, Cu, Ni and V, are
usually lower than in source rocks. Enhanced concentrations
of these metals were recognized only locally or seasonally.
Discrimination of potential sediment sources and identifica-
tion of natural and anthropogenic input can be proved only by
a complex diagnostic approach, because of the natural spatial
variability of source rocks in the fluvial system, the complexi-
ty of sediment transport and delivery processes. The presented
case study shows principles based on which it is possible to
interpret results of sedimentary studies in similar geological
situations.
Acknowledgments: The study was kindly supported by the
research Project MSM 0021622412. The authors would like to
thank O. Lintnerová and two unknown reviewers for their crit-
ical and stimulating comments, which greatly helped improve
the manuscript.
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