Hidrológiai Közlöny 1949 (29. évfolyam)

1-2. szám - E. MOSONYI, D. Eng.: Natural storage effect in the mountainous drainage areras of the Carpathian Basin

. s Palotaírva . 9. Alsó fancsal jo.Málnásfürdö 11 Tokaj .12. Márk-villa .13 Letenye Vizqyiijtöterúkt:km f ' I " 11 I M

II These equations are suitabíe for com.puting ,

f valutes in the mountainous regions of ths Carpathian Basin between the following limits of drainage areas: F=10 km» -:- 10.000 km

2 Of Log F= 1—4. Table I. indicates alsó the theoretical <p values as determined from. equations under (19) and the deviations (in per centage) betwefen actual and theoretical values. Drainage areas adherent to stations 1, 10 and 11 contain regions of different character. It is evident that points belonging to the above stations fali in between the characteristic straight lines. Coefficient f corresponding to drainage areas with rtegions of different character (FA + FB~ F), can be oomputed. by the following formula: VaFA + VBFB » = y <

2

0) where <pa and </>« mean the values on lines A and B respectivtely but referrmg to the whole of the drainage area (F). If specific discharges in heterogeneous regions are different, in place of equation (20) the following: fAgA + 'PBQ

B (21

) QA + IB proportion is to be applied. The examinéd mountainous region consists mainly of the so-calted Carpathian sand-stone (flysch) and, as these regions are of semi-pervious character, in this case <p values for aniy possible extension of the area may vary between 0'844 and 0'506. The author is of the opinion that through the proposed method very reliable results can be reachted if hydrographical data for any excessively dry year are available, even if the year itself is not decisive for temporal distribution of run-off. In this case the totál annual run-off is known and so the necessary reservoir capacity can be computed from (12a), after having dettermined <p from (19) by means of the above mentioned geological maps or through proceedings described in the author's publication (Dr. E. Mosonyi: Hydrological Design of Larger Storage Reservoirs. Budapest, 1948.). Comparison of precipitation data, usually available for a longter period, gives satisfactory control of whether the driest year hydrographically known be really decisive in view of run-off. Hydrographical data are very often far from being complete and so the discharge curve cannot be plotted; and which is worse, for smaller streams even gage observation data are deficient or entirely missing. Consequently the totál run-off of the dry year cannot always be computed directly. Here discharges arte to be determined from precipitation data with regard to the run-off coefficient for the dry year. In his aforementioned study the author has given somé run-off coefficient values for the examined Carpathian region. A far more unfavourable situation is to be faced when precipitation of the driest year cannot be reckoned even from readings of the observing stations in the investigated drainage area. For solving this often occurring alternative, a fairly approximating method is given by the author. After readings for a 15—60 year period of 121 observing stations have been elaborated, it became evident A (p-iOMÍl-^f) B r-t>9S5(l-lj$f) r f> -0-9100-^f) iciboo LoqF s f 10Ü000 Mg. 3. ábra. Varialion of fador f as depmdtng on sise and perviousness of drainage area. A SP tényező értékének váltuaása a vízgyűjtőterület és az áteresztőképesség függvényébon. P Prainage area Vízgyűjtőterület A imperx>ioit,s vízzáró B semi pervious félig áteresztő C perrious áteresztő . i. P 'eiro Vabiszira 1 V/sö I 2 Terebesfejérpatak Tisza

1 . 3. Dombó Tarac . t So/cárja Ta/abor] _íPerecseny Ung .... . ó.CSernoholova Lyuta . ?Jádvölgy Sebes-Körös Maros Görgény Oit 1 Tisza Békás Mura 14