TY - JOUR AU - Nagy, Judit AU - Fiala, K AU - Blanka, Viktória AU - Sipos, György AU - Kiss, Tímea TI - Hullámtéri feltöltődés mértéke és árvizek közötti kapcsolat az Alsó-Tiszán. JF - FÖLDRAJZI KÖZLEMÉNYEK J2 - FÖLDRAJZI KÖZLEMÉNYEK VL - 141 PY - 2017 IS - 1 SP - 44 EP - 59 PG - 16 SN - 0015-5411 UR - https://m2.mtmt.hu/api/publication/3310134 ID - 3310134 LA - Hungarian DB - MTMT ER - TY - JOUR AU - Hernesz, Péter AU - Kiss, Tímea AU - Sipos, György TI - Ártéri szintek és paleo-medrek: ártérfejlődés az Alsó-Tisza mentén JF - FÖLDTANI KÖZLÖNY J2 - FÖLDTANI KÖZLÖNY VL - 145 PY - 2015 IS - 3 SP - 273 EP - 286 PG - 14 SN - 0015-542X UR - https://m2.mtmt.hu/api/publication/2985975 ID - 2985975 N1 - Cited By :1 Export Date: 22 May 2022 LA - Hungarian DB - MTMT ER - TY - JOUR AU - Kiss, Tímea AU - Oroszi, Viktor György AU - Sipos, György AU - Fiala, K AU - Benyhe, Balázs TI - Accelerated overbank accumulation after nineteenth century river regulation works: A case study on the Maros River, Hungary JF - GEOMORPHOLOGY J2 - GEOMORPHOLOGY VL - 135 PY - 2011 IS - 1-2 SP - 191 EP - 202 PG - 12 SN - 0169-555X DO - 10.1016/j.geomorph.2011.08.017 UR - https://m2.mtmt.hu/api/publication/1705596 ID - 1705596 LA - English DB - MTMT ER - TY - CHAP AU - Barabás, Béla AU - Kovács, Sándor AU - Reimann, József TI - Növekednek-e az árvizek? T2 - A Szolnoki Műhely Szemelvények a Vásárhelyi Terv Továbbfejlesztésének megalapozó tanulmányaiból PB - Közép-Tisza-vidéki Vízügyi Igazgatóság (KÖTIVIZIG) CY - Szolnok PY - 2003 SP - 39 EP - 50 PG - 41 UR - https://m2.mtmt.hu/api/publication/32245745 ID - 32245745 LA - Hungarian DB - MTMT ER - TY - JOUR AU - Gábris, Gyula AU - Telbisz, Tamás Ferenc AU - Nagy, Balázs AU - Belardinelli, E TI - A tiszai hullámtér feltöltődésének kérdése és az üledékképződés geomorfológiai alapjai JF - VÍZÜGYI KÖZLEMÉNYEK J2 - VÍZÜGYI KÖZLEMÉNYEK VL - 84 PY - 2002 IS - 3 SP - 305 EP - 322 PG - 18 SN - 0042-7616 UR - https://m2.mtmt.hu/api/publication/1135593 ID - 1135593 N1 - Upsilting of the floodplain of the River Tisza and the geomorphologic basis of the formation of deposits AB - In the Tisza River Basin the recent years were characterised by the enormous increasing of flood level, causing also catastrophes. Peak levels of the floods of 1999 and 2000 have broken all previous records and created a new situation along the River Tisza in which the traditional flood defence practices of continuously increasing the flood levees are not sufficient and not even efficient anymore. There was an urgent need for reconsidering the basic principles of flood control, tailoring and modifying them to suit the new situation. To develop a new concept one needs to know much better the reasons that which caused the increase of flood levels, determining them and proving them. This study deals with a single one of these causes, namely with the rate and spatial distribution of the silting up of the flood-plain. The river reach between Tiszadob and Tiszaszederke?ny, the location of the very first cut-off of a meander during the river regulation, was selected as the study area for this research. The digital topographic map of the area was prepared on the basis of the topographic map of scale 1:10 1000 (Figure I.). The method applied was aimed at the quantitative determination of the extent of the deposition, which resulted on the flood plain during the period of 120 years, elapsed between the time of river regulation and the time of making the map. Two methods were used for the determination of the depth of sedimentation between the levees: The first was based on the values obtained from the sections (profiles), which were drawn perpendicularly to the river. The second was based on the evaluation of indices determined for areas between the profiles. The profiles were taken at about 1 km pacing. Section no 1. was selected downstream of the terrain of higher elevation, to the south of Tiszadob (Figure 1.), in such a way that the adjoining areas outside the levees be also of the old flood-plain type. The last section was at the end of the cut-off, at the present mouth section of the tributary river Sajo?. On the basis of the profiles the average elevation of the terrain on the protected side of the levee was calculated (Figure 2.). These values were considered the base terrain level before river regulation (halap = hbase). The degree of sedimentation was measured relative to this base level (Table I.). Another method was also used for the determination of the average sedimentation depth, calculating the difference between the hhulla?mte?r (hfloodplain), the position of the areas between the sections, and the hbase. (Table II.) The results of the calculation made on the basis of the digital terrain model indicated that the depth of sediment deposition between the sections of the five kilometre long artificial river reach between Tiszadob and the Sajo? mouth varied in the range 0.23-0.60 metres, during the 120 years. This means that the original flood-plain through-flow cross-section was reduced by 5-16%. These results are in harmony with the similar results of others, made by different methods. The differences can be due to the effect of flood-plain erosion, scouring back into the river, and to the compaction of the deposited material. The width of the floodplain can be considered a significant affecting factor. The determination of the morphology of the floodplain (and that of the flood-basin in general) is an important issue from the practical point of view. A similarly important issue is to provide an unambiguous terminology for them. The point bar is formed by the deposition of sediment along the mildly sloping river banks of the convex side of the river bend at falling water level. These sand-bars are the more marked, the slower the side-wise movement of the river bend. Their height decreases parallel to the increase of the water depth from the inner part of the bend towards the concave bank. The crest lines of the point bars are separated from each other by depressions, called the swales (Figure 3.9). When these latter get firstly inundated by the floods they illustratively indicate the series of "o?vza?tony" sand-bars. On the bottom of the o?vza?tonys there are deposits of relatively rough particles (where the sediment originating from the upstream parts of the river might get mixed with the debris originating from the local bank-erosion). Finer inclined layers, getting finer towards the top, are following these rougher bottom deposits. Horizontal clayey-silt layers are found, atop of these inclined layers, at the level of the highest foods. The upstream part of the "o?vza?tony" consists of rougher and more stable material, while the downstream part of finer particles. There might be several other formations along the river, generated in more or less continuous manner. The roughest material (mostly sand) is found right outside of the near-bank zone, where the otuflowing water losses its velocity abruptly. This forms a natural bank-ridge or natural levee along the bank line (Figure 3.). Further off the main channel ever finer particles cover the original terrain. This explains the asymmetry of the ridges, which are steeper towards the main channel and mildly sloping away from it. The degree of development of these natural bank-ridges can be much varying in the middle reach-type meandering river lengths. The can be more developed and higher at the outer, concave side than in the convex one, where they may also be missing. On this side, the zone of the "o?vza?tonys" may be directly transformed into the zone of flood-plain sediments of fine particles. The natural levees are also layered because rising and falling out-flowing waters result in different particle depositions. However, the layers are relatively horizontal ones or follow the mildly arching shape of the bank-ridge. During floods the water flows out at the lowest point of the bank-ridge and the fast flowing water breaks through the natural levee, thus forming the scour channel. The sediment deposited from the out-breaking water (of somewhat rougher particle size than that of the material of the natural levee) forms a smaller delta or crevasse splay on the deepest part of the flood-plain (Figure 3) Formations along the river bank are due not only to the work of the river water. The dry and bare sand surfaces are subject to wind forces that can make them moving over shorter distances. The height of both the point bars and natural levees can be increased by sand: at low water level the dry sand will be moved by the wind, thus increasing their height. The name of these forms is the bank-dune and they have outstanding importance along the River Tisza from both economic and flood-control points of view. They are, however, mostly not developed in our era, but were generated in the near-past of the geological history, in the dry centuries and millennia of the Holocene and the last cold stadials of the glacial period. LA - Hungarian DB - MTMT ER - TY - JOUR AU - Kiss, Tímea AU - Sipos, György AU - Fiala, K TI - Recens üledékfelhalmozódás sebességének vizsgálata az Alsó-Tiszán JF - VÍZÜGYI KÖZLEMÉNYEK J2 - VÍZÜGYI KÖZLEMÉNYEK VL - 84 PY - 2002 IS - 3 SP - 456 EP - 472 PG - 17 SN - 0042-7616 UR - https://m2.mtmt.hu/api/publication/1161019 ID - 1161019 N1 - Nincs jelölve a levelező szerzőség a közleményen. (SE SZTE admin5) LA - Hungarian DB - MTMT ER -