Journal of Environmental Geography 5 (1–2), 29–38. 

RECONSTRUCTION OF PALAEO-HYDROLOGY AND FLUVIAL ARCHITECTURE AT THE 

OROSHÁZA PALAEO-CHANNEL OF RIVER MAROS, HUNGARY 

 
Orsolya Katona

1*
, György Sipos

1
, Alexandru Onaca

2
, Florina Ardelean

2
 

1
Department of Physical Geography and Geoinformatics, University of Szeged, Egyetem u. 2-6, H-6722 Szeged, Hungary 

1
Department of Geography, West University of Timisoara, V. Parvan Str. 4, Timisoara, RO-300223, Romania 

*Corresponding author, e-mail: orsi1983@gmail.com 

Abstract 

Several studies have addressed the impact of climate change and 
tectonic activity on fluvial systems. When investigating these sys-

tems palaeo-hydrological and geomorphological data on abandoned 

channels can yield valuable results. The main aim of our work was to 

reconstruct morphological conditions at the Orosháza palaeo-channel 

and to estimate the bankfull discharge which characterized the chan-

nel during its formation. There are several equations predicting 
bankfull discharge on the basis of planform parameters, but these 

only work for meandering rivers. In case of braided channels flow 

reconstruction can only be made by using cross-sectional parameters. 
The Orosháza palaeo-channel provided the means of a comparative 

analysis in this respect. By a sudden pattern change both meandering 

and braided reaches, supposedly having a very similar bankfull 
discharge, could be simultaneously studied. Planform parameters and 

present cross-sections were determined on the basis of a high resolu-

tion DEM, while original cross-section parameters were assessed 
using sedimentological and geophysical methods. Based on sedimen-

tological data, channel pattern transition was mainly driven by inten-
sive bedload accumulation at the edge of the Maros Alluvial Fan 

(MAF). Slope differences could not be evened out due to an avulsion 

close to the apex of the fan. Concerning discharge calculations a 
good agreement was found between a region-specific planform based 

equation and the cross-section based Grauckler-Manning equation. 

Values determined for the braided and meandering reach were also in 
a good correspondence. Consequently, the presented approach is 

suitable to determine the discharge of other braided palaeo-channels 

on the MAF and elsewhere.  

Keywords: morphological reconstruction, hydrological recon-

struction, sedimentology, geophysics, discharge equations 

INTRODUCTION 

The reconstruction of fluvial systems is of key importance 

if the climatic variations or tectonic development of an 

area is investigated. Therefore in the past decades numer-

ous studies have been made to investigate past fluvial 

architecture, morphology and sedimentology at various 

locations (e.g. Dury, 1976; Sridhar, 2007; Timár and 

Gábris, 2008). When studying ancient fluvial systems one 

of the basic approaches is to allocate and investigate 

abandoned channels still detectable on the surface. These 

provide information primarily on Late Pleistocene and 

Holocene changes in the environment (Carlston, 1965; 

Bridge, 2003). Based on the morphometry and sedimen-

tary structure of these channels various conclusions can be 

made on the discharge of the forming river and the quality 

and quantity of its sediment. These in turn might provide 

information to the development of contemporary topogra-

phy and palaeo-climatic conditions. The interpretation of 

surficial and shallow deposits is either based on in situ 

observations, laboratory experiments or geophysical 

methods (Bridge, 2003; Sridhar, 2007). 

The fluvial network of the Pannonian Basin has 

been affected in the past by climate variations and dif-

ferent rate of tectonic subsidence and uplift processes, 

the effect of base level change can be regarded negligible 

(Bridge, 2003; Timár et al., 2005; Gábris and Nádor 

2007; Nádor et al. 2007). Tectonic processes are primari-

ly important in determining the gradient and the direc-

tion of the flow of rivers (Bridge, 2003; Laure, 2008). As 

the tectonic development of the Pannonian Basin has 

been very complex, the reconstruction of the changes in 

the fluvial network since the regression of the Pannonian 

Lake still poses some questions (Gábris et al., 1986) in 

case of the Maros River system as well  (Mike, 1991). 

Climatic factors, such as mean annual temperature and 

annual precipitation have an influence on channel pattern by 

determining runoff the type of weathering and vegetation 

cover (Schumm, 1985; Mackey, 1993; Bridge, 2003). In the 

temperate zone the dimensions of a fluvial system is usually 

adjusted to annually or biannually returning floods, howev-

er under changing climatic conditions the role of single, 

extreme events may be much more significant (Schumm, 

1985; Bridge, 2003). Nevertheless, in terms of alluvial 

rivers the role of bankfull discharge is stressed as channel 

forming processes are related mostly to these in various 

works (Leopold and Wolman, 1957; Richards, 1982; 

Schumm, 1985; Bridge, 2003). In the Pannonian Basin, 

located in a climatic transition zone, variations could be 

significant in the past and could result tremendous changes 

in the dimensions and capacity of lowland rivers (Gabris, 

1986). However, climate change and tectonic activity can 

be equally apparent and it is particularly difficult to know if 

a sedimentological and morphological change is due to 

which of the above controlling factors. (Krzyszkowski, 

1996; Bridge, 2003; Vanderberghe, 2003).  

Recent activity in data collection on present day 

rivers has allowed on many parts of the world to de-

velop equations which can be applied to reconstruct 

past discharge values (Bridge, 2003). The relationship 

between discharge and planform parameters is well 

demonstrated in case of meandering rivers (Williams, 



30 Katona et al. (2012)  

 

1984; Bridge, 2003). Parameters mostly used for the 

reconstruction are chord length, radius of meander and 

wavelength of meandering (Williams, 1984). These 

parameters are sometimes not easy to assess, due to the 

low number of detectable palaeo-channels, or blurred 

morphology. Discharge calculations of this type obvi-

ously will not work on straight or braided rivers. 

Another approach for determining discharge is the 

application of hydraulic parameters, such as area of 

cross-section, slope, grain size and roughness. Rela-

tionships of this type are more or less based on the 

classical equation determined by Gauckler and Man-

ning (1890s). The Gauckler-Manning equation has been 

reworked by several authors to fit to different channel 

patterns and different sets of empirical data (Lane, 

1957; Leopold and Wolman, 1957; Osterkamp, 1978; 

Begin, 1981), however the original equation is still 

widely used in the literature (Bridge, 2003). When 

applying hydraulic parameters for the discharge calcu-

lations of palaeo-channels it is of major concern to 

determine values of original slope and cross-sectional 

area. In these investigations the role of topographical 

and sedimentological measurements is inevitable, how-

ever shallow geophysical methods, such as ground 

penetrating radar (GPR), or electrical resistance tomog-

raphy (ERT) can be also efficient if environmental 

conditions are suitable (Gourrya et al., 2003; Carreon-

Freyer et al., 2003; Bersezio et al., 2007; Van Dam, 

2010; Yadav et al., 2010; Rucker et al., 2011) 

Considering the above, the first aim of our study 

was to test morphological and hydraulical equations on 

a braided and meandering palaeo-channel section locat-

ed on the alluvial fan of the Maros River in Hungary. 

For the calculations planimetric, topographic, 

sedimentological and geophysical data were applied. 

Henceforth the potential of different geophysical met h-

ods could be assessed. Finally, we aimed to calculate 

an average bankfull, or channel forming discharge, 

characterising the investigated palaeo-channel reach. 

STUDY AREA 

The study area is located on the interfluve area bor-

dered by the Tisza, Maros and Körös rivers. Geomor-

phologically, the territory is primarily dominated by the 

alluvial fan of the Maros River (Pécsi, 1959). The Ma-

ros Alluvial Fan (MAF) with a total area of 10 000 km
2
 

hosts numerous palaeo-channels, representing Late 

Glacial, Holocene river generations of the Maros 

(Borsy, 1989; Molnár, 2007; Sipos et al., 2012). From 

these, one of the largest palaeo-channel is located in the 

axis of the alluvial fan, near its western edge at the 

town of Orosháza (Fig. 1). 

The present day catchment of the river is 30 000 

km
2
, most of which is located in the Transylvanian Ba-

sin, the Eastern and Southern Carpathians (Molnár, 

2007). There are no signs for significant changes in the 

size of the upland catchment during the Quaternary 

(Mike, 1991). On its lowland reach the Maros has built a 

large alluvial fan during the Late Pliocene and Pleisto-

cene with a radius of 80-100 km starting from the Lipova 

gorge. Changes in the direction of its flow on the fan 

were caused partly by tectonic (local uplifts and subsi-

dences) and geomorphological (avulsion) factors (Borsy, 

1989). The apex of the fan is at 130 m asl while its rim is 

between 80-85 m asl. The slope of the fan is not uni-

form, usually it is between 20 and  30 cm/km however 

near the edge there is a belt where it can reach occasion-

ally 50 cm/km (Sümeghy and Kiss, 2011).  

Thanked to the above, the river has a relatively high 

energy which is also resembled by the high sediment 

transport capacity of the present-day Maros, which is 

similar to that of the Tisza or the Danube. Horizontally, 

the sediment of the MAF changes from primarily gravel 

near the apex to sand and silt towards the edges (Borsy, 

1989). Vertical variations in the granulometry of the fan 

sediment are related to Pleistocene climatic changes in 

general, namely coarser and finer strata referring to gla-

cial and interglacial phases, respectively (Mike, 1991; 

Molnár, 2007). 

The Hungarian part of the MAF can be divided into 

four geomorphological subunits based on surface forms 

and sediments (Pécsi, 1959). The central part is covered 

by sandy loess and dominated by meandering palaeo-

channels (Fig. 1). The NE wing is mainly composed of 

alluvial loess and silt deposits and hosts both meandering 

and braided palaeo-channels. The northern edge just 

south of the Körös Basin is covered with sandy loess and 

primarily braided channel forms are characteristic. Fi-

nally the western wing has alluvial loess on the surface 

and meandering channels. 

The site of the investigation at Orosháza is right at 

the edge of the alluvial fan. East of the town the almost 1 

km wide channel has a braided pattern with several sub 

channels and huge bar forms. Downstream the same 

channel after leaving the edge of the fan becomes mean-

dering, its width decreases at certain sections to only a 

few 100 m. According to results of OSL dating the 

Orosháza channel was active during the Pleistocene- 

Holocene shift, between 14 and 8 ka (Sipos et al., 2012). 

As a consequence, post formational loess deposition 

could not be significant. Partly because of this and due to 

supposedly fast avulsion processes (Sümeghy and Kiss, 

2011) forms are still sharp and well detectable. For the 

present research two study sites were investigated, one 

on the braided, the other on the meandering section of 

the palaeo-channel (Fig. 1). 



 Reconstruction of palaeo-hydrology and fluvial architecture at the Orosháza palaeo-channel 

of River Maros, Hungary 

31 

 

 
Fig. 1 Location of the study area and the Geomorphological Map of the region (based on Pécsi, 2000) 



32 Katona et al. (2012)  

 

METHODS 

As a first step a digital elevation model (DEM) was 

produced from 1:10000 scale topographic maps with 1 m 

interval primary contour lines, supplemented by 0.5 m 

interval secondary contour lines on flat areas. The DEM 

was made with the ArcGIS Topo to Raster interpolation 

tool. Vertical resolution was better than 1 m, while hori-

zontal raster resolution was 10 m (Fig. 2). The DEM was 

used to determine channel planimetric parameters (me-

ander wavelength, meander radius), present day silted up 

cross-sectional parameters (width, deth, area), and chan-

nel slope conditions on the investigated palaeo-reach. 

Cross-sectional indicators were measured at various 

points in order to get average parameters. The area’s 

general slope was calculated on the basis of SRTM data. 

Since the DEM enabled only the calculation of 

modified, silted up cross-sectional parameters other 

methods also had to be applied and compared to deter-

mine the original dimensions of the river. The primary 

aim was to determine the depth of channel sediments and 

calculate the true depth of the river. In all 16 drillings 

were made in two cross-sections representing both the 

braided and the meandering reaches (Fig. 2). Drillings 

were representing characteristic topographic features, 

such as the natural levee, river bed, bar crests, point bars 

and chutes. Bore holes were deepened till the level of the 

groundwater. The depth of the drillings in the channel 

was 1.5-2 m, on point bars and levees 5-6 m. Samples 

were taken at every 10 cm. Sedimentological analysis 

included grainsize analysis. The grainsize-distribution of 

the samples was determined by a Fritsch Analysette 22 

laser equipment with a measurement range of 0.08-2000 

μm. Samples underwent ultrasonic homogenisation and 

all measurements were repeated three times to check if 

there is further disintegration. For the geomorphological 

interpretation sample D50 values were determined. 

In order to test the applicability of geophysical 

methods in determining sedimentary shifts GPR and 

ERT were applied in the drilling sections (Fig. 3). GPR 

measurements were made with a GSSI type instrument, 

using 200 and 270 MHz shielded antennae. 

Unfortunately right during the first field work it turned 

out that sedimentary conditions (high clay and silt 

content in the upper strata) disable the successful use of 

GPR technology on these sites. Therefore, ERT profiling 

was favoured during later measurements. For these 

measurements a PASI type 32 electrode system was 

used. ERT sections were measured using a Wenner 

electrode array. Electrode spacing was 5 m, one section 

 
Fig. 2 DEM generated from 1:10000 scale topographic maps with the cross-sections studied in detail 



 Reconstruction of palaeo-hydrology and fluvial architecture at the Orosháza palaeo-channel 

of River Maros, Hungary 

33 

 

was therefore 160 m, from these 5 were measured on 

both sites. Neighbouring sections had a 50 % overlap. 

Maximum penetration was 20-30 m, data were collected 

from 10 levels. 

From a geomorphological aspect bankfull discharge 

is one of the most important parameter of river flows, as 

it is highly responsible for the geometry of the cross-

sections and the channel pattern as well (Schumm, 

1985). Bankfull discharge was assessed by selecting and 

using equations from the literature, with special attention 

to the range of applicability of the published formulae. 

In terms of planimetric parameters the equations of 

Leopold and Wolman (1957) and Mackey (1993) were 

selected (Table 1). These formulae can be applied only 

for meandering channels, and they use meander wave-

length as the base parameter. The relevance and signifi-

cance of meander wavelength was also reinforced by 

Timár and Gábris (2008) when studying the channels of 

the Great Hungarian Plain. The selected formulae oper-

ate up till the 1000 m
3
/s discharge range, thus proved to 

be adequate as a first approximation. 

Discharge calculations were also made from cross-

sectional parameters. At the two measurement sites these 

were derived from DEM (present) and sedimentological 

(original) analyses, results were compared and coefficients 

were calculated. These coefficients were used to calculate 

average original cross-section parameters from representa-

tive present-day values calculated by taking the mean and 

standard deviation of several measurements on the DEM. 

In case of the meandering section the relationships 

determined by Dury (1976) and Williams (1978) were 

tested. The range of the applicability of the Williams 

(1978) formula (0.5<Qb<28320m
3
/s; 0.7<Ab<8510m

2
; 

0,000041<s<0,081) is well over the expected discharge 

of the investigated system (Table 1). In terms of the 

braided reach the modified Gauckler-Manning equation 

was applied. The basic equation (Q=AR
2/3

S
1/2

/n) was 

modified and reduced by Rotnicki (1983) based on more 

than 1000 observations on rivers with highly variable 

geometry (Q=(1,49/n)wd
5/3

sc
1/2

). Parameter “n” was 

determined after Goodwill and Sleigh (2002), and calcu-

lations made on the basis of present-day measurements 

on River Maros (Katona et al., 2012). The average value 

used for calculations was 0.056. 

RESULTS  

Sedimentological and geomorphological interpretation 

The original channel cross-sections were recon-

structed on the basis of sedimentological data and 

geophysical measurements. Channel sediments can be 

clearly identified in the sedimentary columns, thus the 

amount of silting up in the thalweg zone can be est i-

mated to be approximately 2-3 m (Fig. 4). Silting up 

is suggested to be the result of post-formational flu-

vial activity as from time to time the channel could be 

partially reactivated during the extreme floods of the 

   
Fig. 3 Geophysical field investigations. The bank of the braided section on the left, and bank of meandering on the right. 

Table 1 Equations applied for the calculation of bankfull discharge 

meandering author equation 

planform 

Leopold and Wolman (1957) L=65.2Qb
0,5

 

Mackey (1993) L=72.16Qb
0,49

 

Sümeghy and Kiss (2011) Q = 0.0003*L
2
+0.3440*L-81.329 

cross-section 
Dury (1976) Qb=9.93 Ab

0,85 

Williams (1978) Qb=4.0Ab
1,21

sc
0,28

 

braided author equation 

cross-section Grauckler-Manning  Q=wd
5/3

sc
1/2

*1.49/n 



34 Katona et al. (2012)  

 

Maros system. Natural levees, point bars and mid 

channel bars are still sharply detectable. We took the 

present level of these as the minimum heights of 

banks as subsequent erosion and agricultural activity 

could lower their level. The D50 value of overbank, or 

suspended sediments is similar at the two study sites, 

being 25-30 and 20-25 μm in the braided and the me-

andering corss-section, respectively (Fig. 4). Never-

theless, there is an abrupt change in the grainsize of 

the bedload. On the braided section the D50 value of 

channel sediments is 200-300 μm, representing the 

range of coarse grain sand. Meanwhile, less than 15 

km downstream on the meandering section, mean 

grainsize decrease to 50-150 μm. The degree of sort-

ing however also decreases, but this is due to the ap-

pearance of clayey fractions in channel sediments.  
 

In terms of channel slope and general slope it turns 

obvious that the upstream braided section has a 15-20 % 

lower slope than the downstream meandering one (Table 

2). The knick point signs the transition between channel 

patterns. Such change in slope is unusual in terms of 

normal gradient alluvial rivers (e.g. Schumm, 1985; 

Richards, 1996). In this case a possible cause could be 

tectonic activity, however, this does not explain the sig-

nificant change in the composition of channel sediments. 

Pattern and slope change is rather caused by the geo-

morphological background, i.e. the knick point marks the 

edge of the alluvial fan.  

 
Fig. 4 Cross-section of the sites with sedimentary sequences of drillings and generalised ERT profiles 



 Reconstruction of palaeo-hydrology and fluvial architecture at the Orosháza palaeo-channel 

of River Maros, Hungary 

35 

 
By reaching the distal parts of the fan the compe-

tence and capacity of the river, having a very high bed 

load of coarse sand, decreased considerably, leading to 

the development of an aggradation zone (braided sec-

tion). Downstream of this zone slope and energy in-

creased, and as the river already deposited its coarse 

sediment upstream, meandering was favoured. Meander-

ing could be further facilitated by sedimentological dif-

ferences, i.e. in front of the coarser alluvial fan sedi-

ments finer more cohesive floodplain deposits are lo-

cated, confining the banks of the channel (Fig. 1 and 4).  

Difference in slope suggests a difference in cross-

sections as well, namely, larger slope means smaller 

cross-section at similar discharge on the same river. Data 

have reinforced this relationship (Table 2). The average 

cross-section of the braided and meandering reaches 

could be around 3000 and 3800 m
2
, respectively. 

Width/depth ratios also show a remarkable difference 

between the two sections, being around 400 on the 

braided and 130 on the meandering section. 

Geophysical interpretation 

In an alluvial setting the electric resistance threshold 

between sedimentary units is hard to determine, as dif-

ferent sediments can have very similar resistance (Rey-

nolds, 1997). In general however, the coarser and drier 

the sediment the higher resistance is received. The study 

area is primarily characterised by mixed silt, fine and 

medium sand, which made the interpretation of ERT 

profiles complicated. 

The ERT measurements were made in autumn 

among dry conditions, thus precipitation could not influ-

ence resistivity parameters near the surface (Reynolds, 

1997). The received values were between 0 and 300 Ωm. 

As a first approximation the threshold between silt and 

sandy sediments was based on the values reported by 

Nádor et al. (2005) and Yadav et al. 2010, and was taken 

20 Ωm. Resistivity profiles however could not entirely 

be compared to the drilling profiles, due to the resolution 

provided by the 5m electrode spacing. Nevertheless, in 

case of Site 1 (Fig. 5) the top layers, especially near the 

bank of the channel, were dominated by sediments with 

high resistance down till 10-15 m (75-80 m asl). Note 

that ground water appeared at around 85 m asl, therefore 

the change experienced in this case is primarily due to 

changes in grainsize, meaning that coarser sandy sedi-

ments are deposited on finer clayey deposits. High resis-

tivity strata wedge out towards the centre of the channel. 

At Site 2 resistivity values were a little higher in gen-

eral (Fig. 6), which seems to contradict the hypothesis that 

sedimentary deposits are finer in front of the alluvial fan. 

Contradiction can only be relieved if we suggest that the 

mineral composition of sediments at the two sites is slightly 

different. This hypotheses however needs further testing. 

Nevertheless, relative differences of the Site 2 profile show 

an opposite pattern than that of Site 1 profile. Lower than 

20 Ωm values appear on the top left, while higher resistivity 

values characterise sediments 5-10 m below the surface. As 

the boundary is again beneath the ground water table it is 

obvious that palaeo-channel sediments were laid on coarser 

deposits. Lateral bar surfaces in the middle of the cross 

section have higher resistivity similar to point bar sediments 

on the right (Fig. 6). Based on these data, the boundary 

surface might represent the base of the palaeo-channel, 

although the 20 Ωm threshold needs to be revised in light of 

higher resolution ERT results. In all, further calculations 

were based on the results yielded by sedimentological 

analysis, at present resistivity profiles are not precise 

enough to draw unambiguous sedimentary boundaries. 

Palaeo-discharge calculations 

Bankfull discharges calculated by different approaches 

showed considerable variance (Table 3). In terms of the 

meandering reach discharges calculated on the basis of 

Table 2 Cross-sectional parameters of the investigated sites 

 Site 1 (braided) Site 2 (meandering) 

L (m) - 2500 ± 600 

s (cm/km) 25.6 ±1.3 29.7 ± 1.0 

sc (cm/km) 20.3 ± 0.3 22.5 ± 1.0 

 Parameters of the investigated cross-sections 

 DEM drilling coeff. DEM drilling coeff. 

w (m) 1125 1125 1,00 685 685 1.00 

d (m) 2,3 2,8 1,21 3,15 4,20 1.33 

Ab (m
2
) 2345 3150 1,34 2076 2870 1.38 

 Average values based on several measurements on the DEM 

 DEM original DEM original 

average w (m) 1120 ± 140 1120 ± 140 595±80 595±80 

average d (m) 2,2±0,32 2,7 ± 0,7 3,05±0,7 4,05±0,9 

average Ab (m
2
) 2465±470 3025 ± 870 1815±480 2410±625 

L: meander wavelength, s: general slope, sc: channel slope, w: width, d: deep, Ab: area of bankfull cross section 



36 Katona et al. (2012)  

 

the classical planform equations (Leopold and Wolman, 

1957; Mackey 1978) were considerably, almost 50 % 

lower than the value received using the region-specific 

formula of Sümeghy and Kiss (2011). By using the equa-

tion of Dury (1976), setting up a relationship between 

discharge and cross-sectional area in case of meandering 

rivers, the received result was clearly and significantly 

overshooting the previous values. When slope was intro-

duced to the relationship (Williams, 1978) the estimated 

discharge decreased, but it was still significantly higher 

than the values derived from planform parameters. By 

applying the modified Gauckler-Manning equation the 

calculated discharge was very close to the results yielded 

by the Sümeghy and Kiss formula. Based on this, we 

assume that the two approaches reinforce each other and 

the bankfull discharge of the river on the meandering 

section was approximately 2500 m
3
/s. 

In case of the braided section the only way to de-

termine bankfull discharge was to use the Gauckler-

Manning equation. In theory the result received for this 

section should be similar to that calculated for the mean-

dering reach. As a matter of fact, results were fairly well 

corresponding, fell within the error limits and there was 

only a 9 % difference between the mean values. Conse-

quently, the Gauckler-Manning equation seems to be 

suitable to determine bankfull discharge values on 

braided channel section on the MAF. It has been proved 

however that classical planform formulae significantly 

underestimate, while cross-section based formulae over-

estimate the discharges in this environment. One reason 

can be, that based on width/depth ratios the channels – 

even those meandering – of the MAF are transitional. 

If we compare the received values to the present-

day bankfull discharge (850 m
3
/s) of the Maros River 

(Fiala et al., 2007), there is a considerable difference, 

referring to a much different flow regime during the 

onset of the Holocene. 

Table 3 Bankfull discharge values calculated from planform 

and original cross-sectional parameters. 

Equation Site 1 Site 2 

Leopold and 

Wolman (1957) 
 1470 ± 350 m

3
/s 

Mackey (1993)  1390 ± 330 m
3
/s 

Sümeghy and 

Kiss (2011) 
 2650 ± 630 m

3
/s 

Dury (1976)  7280 ± 1980 m
3
/s 

Williams (1978)  4570 ± 1240 m
3
/s 

Gauckler - 

Manning 
2220 ± 640 m

3
/s 2445 ± 645 m

3
/s 

CONCLUSIONS 

The Orosháza palaeo-channel system provided a good 

opportunity to test different field and computational 

methods for determining the bankfull discharge of me-

andering and braided channel sections. The complex 

analysis included geomorphological, geophysical and 

sedimentological methods, and emphasizes the necessity 

of comparing these results. 

Based on the investigations some important geomor-

phological results could be drawn. First, a discrepancy 

between slope and channel pattern was experienced on the 

area, which is probably due to inherited slope conditions 

and high bed load deposition near the edge of the MAF. 

This suggests that as a matter of an avulsion event the 

studied channel was not operating as a main flow path for 

a long time, i.e. channel slopes could not be adjusted to 

different general slope values. Since their formation the 

channel silted up 2-3 m, meaning that the forms studied 

are fairly young, thus the effect of post formational tec-

tonic changes might be also of secondary importance. 

At the present phase of research sedimentological 

and geophysical profiles could not entirely be over-

 

Fig. 5. ERT profiles at Site 1 

 
Fig. 6. ERT profiles at Site 2 



 Reconstruction of palaeo-hydrology and fluvial architecture at the Orosháza palaeo-channel 

of River Maros, Hungary 

37 

 
lapped, as a matter of their different vertical extent and 

resolution. However, ERT profiling seems to have a 

great potential in the fast detection of sedimentary struc-

tures on the study area if electrode spacing is decreased. 

GPR measurements failed due to the high clay and silt 

content of the sediments. 

Discharge calculations on the meandering and 

braided reaches showed an acceptable agreement. In case 

of the meandering reach the results based on the mean-

der wavelength/bankfull discharge formula of Sümeghy 

and Kiss (2011) and those derived from the Gauckler-

Manning equation reinforced each other. Moreover, the 

value received for the braided reach was also in a good 

correspondence, meaning that cross-sectional parameters 

determined from sedimentological results can have an 

important role in estimating the bankfull discharge of 

braided channels on the MAF. 

In all, the calculated bankfull discharges suggest 

much higher energy fluvial processes than today. Consid-

ering the age and the dimensions of the Orosháza palaeo-

channel, and also taking into account that the area of the 

Maros catchment has not changed in the past 10-15 ka, we 

can suggest that high discharges were mainly related to 

the melting of glaciers in the upland drainage basin. 

Acknowledgements 

The research was supported by HURO/0901/266/2.2.2 

project. 

References 

Begin, Z.B. 1981. The relationship between flow shear stress and 

stream pattern, Journal of Hydrology 52, 307–319. 
Bersezio, R., Giudici, M., Mele, M. 2007. Combining sedimentological 

and geophysical data for high-resolution 3-D mapping of fluvial 

architectural elements in the Quaternary Po plain (Italy), 
Sedimentary Geology 202, 230–248. 

Borsy, Z. 1989. Az alföld hordalékkúpjainak negyedidőszaki fejlődés-

története, Földrajzi Értesítő 38 (3–4), 211–224. 
Bridge, J.S. 2003. Rivers and floodplains: Forms, Processes and 

Sedimentra record, Blackwell Science Ltd. Oxford 

Carlston, C.W. 1965 The relation of free meander geometry to stream 
discharge and its geomorphic implications; American Journal of 

Science 263, 864–885. 

Carreon-Freyer, D., Cerca, M., Hernandez-Marin, M. 2003. Correlation 
of near-surface stratigraphy and physical properties of clayey 

sediments from Chalco Basin, Mexico, using Ground Penetrating 

Radar, Journal of Applied Geophysics 53, 121–136. 
Dury, G.H. 1976. Change prediction, present and former, from channel 

dimensions. Journal of Hydrology 30, 219–245.  

Fiala, K., Sipos, Gy., Kiss, T., Lázár, M. 2007. Morfológiai változások 

és a vízvezető-képesség alakulása a Tisza algyői és a Maros ma-

kói szelvényében a 2000. évi árvíz kapcsán. Hidrológiai Közlöny 

87 (5), 37–46. 
Gábris, Gy. 1986. Alföldi folyóink vízhozamai, Alföldi tanulmányok 

10, 35–52 

Gábris, Gy.,  Nádor, A. 2007. Long-tern fluvial srchives in Hungary: 
response of the Danube and Tisza rivers to tectonic movements 

and climatic changes during the Quarternary: a review and new 

synthesis, Quarternary Science Reviews 26, 2758–2782. 

Goodwill, I. M., Sleigh, P.A. 2002, Fluid mechanics, Open channel 
Hydraulics, 

http://www.efm.leeds.ac.uk/CIVE/CIVE2400/OpenChannelHydr

aulics2.pdf; available: 2013 jan. 
Gourrya, J.C., Vermeersch, F., Garcin, M., Giot, D. 2003. Contribution 

of geophysics to the study of alluvial deposits: a case study in the 

Val d’Avaray area of the River Loire, France, Journal of Applied 
Geophysics 54, 35–49. 

Katona, O., Sipos, Gy., Nagy, Z. 2012. A Maros hordalékkúp elhagyott 

medreinek hidromorfológiai és hidrodinamikai jellemzői, A Ma-
gyar Földrajzi konferencia Tanulmánykötete, ISBN 978-963-306-

175-6. 
Krzyszkowski, D. 1996. Climatic control on quartenary fluvial 

sedimentation in the Kleszczow graben, Central Poland, 

Quarternary Science Reviews 15, 315–333. 
Lane, E.W. 1957. A study of the shape of channels formed by natural 

streams flowing in erodible material. Missouri River Division 

Sediment Series No. 9, U.S. Army Engineering Division Missouri 

River, Corps of Engineers, Omaha, Nebraska. 

Laure, J.P. 2008. Tectonic influences on the Quarternary drainage 

evolution ont he north-western margin of the French Central 
Massif: The Creuse valley example, Geomorphology 93, 398–

420. 

Leopold, L.B., Wolman, M.G. 1957. River Channel patterns: braided, 
meandering and straight, Geological Survey Professional Paper 

282-B, United States Goverment Printing Office, Washington 

Mackey, S.D. 1993. Theoretical modeling of alluvial architecture. PhD 
thesis, State University of New York, Bringhamton, NY. 

Mike, K. 1991. Magyarország ősvízrajza és felszíni vizeinek története, 

Aqua Kiadó, Budapest, 698 p. 
Molnár, B. 2007.  A Maros folyó kialakulása és vízgyüjtő területének 

földtani felépítése, Hidrológiai Közlöny 87(2) 27–30.  

Nádor, A., Thamó-Bozsó, E., Magyari, Á., Babinszki, E. 2007. Fluvial 
response to tectonic and climate change during the late 

Weichselian in the eastern part of the Pannonian Basin (Hunga-

ry), Sedimentary Geology 202, 174–192 
Osterkamp, W.R. 1978, Gradient, discharge, and particle-size relations 

of alluvial channels of Kansas, with observations on braiding: 

American Journal of Science 278, 1253–1268. 
Pécsi, M. 1959. A magyarországi Duna-völgy fejlődéstörténete, 

(Entwicklung und Morphologie des Donautales in Ungarn), Aka-

démiai Kiadó, Budapest, 346 p. 
Reylnolds, J. M. 1997. An introduction to applied and environmental 

geophysics, John Wiley & Sons Ltd. Baffins Lane, Chichester, 

West Sussex PO 19 1UD, England. 
Richards, K.S. 1982. Rivers, form and process in alluvial channels. 

Methuen, New York. 

Richards, K.S. 1996. Samples and cases: generalisation and 
explanation in geomorphology. In: Rhoads, B.L., Thorn, C.E. 

(Eds) The scientific nature of geomorphology, Wiley, Chichester,  

171–190.  
Rotnicki, K. 1983. Modelling past discharges of meandering rivers. In 

Gregory, K. J. (ed.) Background to Palaeohydrology. Wiley, 

Chichester, 321–354. 
Rucker, D.F.,  Noonan, G.E.,  Greenwood, W.J. 2011. Electrical 

resistivity in support of geological mapping along the Panama 

Canal, Engineering Geology 117, 121–133. 
Schumm, S.A. 1985. Patterns of Alluvial Rivers. Annual Review of 

Earth and Planetary Sciences 13, 5–27. 

Sipos, Gy., Kiss, T., Sümeghy, B., Urdea, P. Tóth, O., Katona, O., 
Onaca, A. 2012. Late Pleistocene-Holocene development of the 

Maros alluvial fan, Hungary-Romania, revealed by luminescence 
dating. UK Luminescence and ESR meeting, Aberyswyth, Book 

of Abstracts. 

Sridhar, A. 2007. Discharge estimation from planform characters of the 
Shedhi River, Gujarat alluvial plain: Present and Past, Journal of 

Earth System Science 116 (4), 341–346.  

http://www.efm.leeds.ac.uk/CIVE/CIVE2400/OpenChannelHydraulics2.pdf
http://www.efm.leeds.ac.uk/CIVE/CIVE2400/OpenChannelHydraulics2.pdf


38 Katona et al. (2012)  

 

Sümeghy, B., Kiss, T. 2011  Discharge calculation of the 

paleochannels on the alluvial fan of the Maros River, Hungary, 
Journal of Environmental Geography 4 (1–4), 11–17 

Timar, G., Gábris, Gy. 2008. Estimation of water conductivity of the 

natural flood channels on the Tisza flood-plain, the Great 
Hungarian Plain, Geomorphology 98, 250-261 

Timar, G., Sümegi, P., Horváth, F. 2005. Late Quarternary dynamics of 

the Tisza River: Evidence of climatic and tectonic controls, 
Tectonophysics 410, 97–110. 

Vandenberghe, J. 2003. Climate forcing of fluvial system development: 

an evolution of ideas, Quarternary Science Reviews 22, 2053–
2060.  

Van Dam, R.L. 2010. Landform characterization using geophysics - 

Recent advances,  applications, and emerging tools,  
Geomorphology 137 (1), 57–73 

Williams, G.P. 1984. Developements and applications of 

geomorphology, Springer-Verlag Berlin Heidelber. 
Yadav, G.S., Dasgupta, A.S., Sinha, R., Lal, T., Srivastava, K.M., 

Singh, S.K. 2010. Shallow sub-surface stratigraphy of interfluves 

inferred from vertical electric soundings in western Ganga plains, 
India Quaternary International 227 (2), 104–115.