2018 | 71/2 | 65–81 | 6 Figs. | 2 Tabs. | 3 App. Tabs. | www.geologia-croatica.hr Journal of the Croatian Geological Survey and the Croatian Geological Society 1. INTRODUCTION The excessive application of chemical fertilizers and manures to agricultural lands has increased the influx of substances into the ground, which eventually reach and contaminate groundwater (SPALDING et al., 1982; UMEZAWA et al., 2008; ZHANG et al., 2014). In order to identify the type of contamination, deter- mine its extent, trace the source and extract valuable information about the groundwater such as its age, the water is sampled to measure stable isotope ratios, major and minor ion concentrations as well as trace metals. Water and substances reaching aquifers serve as a guide to determining these groundwater characteristics (DEMLIE et al., 2007; CLOUTIER et al., 2008; HOSONO et al., 2014). Usually in groundwater studies, a direct link is created be- tween the characteristics of the groundwater and ions, isotopes and metals on the surface without taking the unsaturated zone into consideration even though substances pass through this zone before reaching groundwater. Although the unsaturated zone has not been as actively studied as groundwater, studies have been carried out over the years that give some insight into the flow pro- cesses and solute behaviour through it (BEVEN et al., 1982; GUYMON, 1994; LIN et al., 2006). General unsaturated flow processes have also been studied. Field experiments using Cl- as a tracer were conducted on a mine waste pile (5 m high) to eva- luate the infiltration rate and detect the dominant flow system in the pile (NICHOL et al., 2005). NIMMO et al. (2007) modelled unsaturated zone flow using soil science and hydrologic data. The Evaluations of the downward velocity of soil water movement in the unsaturated zone in a groundwater recharge area using δ18O tracer: the Kumamoto region, southern Japan Azusa Okumura1*, Takahiro Hosono1, Dennis Boateng2 and Jun Shimada1 1 Kumamoto University, Priority Organization for Innovation and Excellence, 2-39-1 Kurokami, Kumamoto 860-8555, Japan; (*corresponding author: osnx.2157@gmail.com) 2 Kumamoto University, Graduate School of Science and Technology, 2-39-1 Kurokami, Kumamoto 860-8555, Japan doi: 10.4154/gc.2018.09 Abstract Water and substances from the surface infiltrate the unsaturated zone before reaching ground- water. Yet, little study has been done on the unsaturated zone due to the difficulty of sampling. A lot of studies have been carried out on the top soil down to a depth of one metre and on shal- low aquifers because they are easily accessible for sampling. The unsaturated zone of the Ku- mamoto region recharge areas is important due to concerns about groundwater pollution from agriculture. The aim of this study was to estimate the downward velocity of soil water movement through the unsaturated zone and the recharge rate using δ18O as a tracer. Five sampling sites were selected and a core was taken from each site. The cores were cut into 0.1 m pieces and soil water was extracted from each to analyze for δD and the δ18O content. Average δD and δ18O compositions of soil water were similar to the isotopic compositions of summer precipitation. An- nual average recharge rate and the downward velocity of soil water in each site were estimated by fitting a vertical δ18O profile pattern to a precipitation δ18O time series as a theoretical water displacement flow model for recharge. An estimated annual average recharge rate in the re- charge area ranged from 745 to 1058 mm/yr with the annual average downward velocity of 1.37 to 2.34 m/yr. Based on the estimated downward velocity, the infiltration time for soil water to reach the aquifer was determined as ranging from 9 to 24 years, which corresponds with previ- ous groundwater age estimations presented in an earlier published study on the same area. It was assumed that contaminants will reach aquifers in 9 to 25 years if the effects of diffusion and microbiological reaction are not taken into account. study focused on preferential flow and the general transport time was also clarified. DELIN et al. (2017) applied rhodamine and Br tracers to a crude oil contaminated site to detect the influence of oil on the water infiltration rate in the unsaturated zone. These studies show that the plurality of flow processes such as prefe­ rential flow and matrix flow complicates water infiltration and contaminant behaviour through unsaturated media. Understand- ing the behaviour of water in the unsaturated zone is important for making decisions about groundwater usage and formulating mitigation measures against groundwater contamination. One of the earliest soil water studies using water stable iso- topes was performed by ZIMMERMANN et al. (1966). In this study, D2O was sprayed on the study area as a tracer. Soil down to 1.2 m depth was sampled 4, 26, 82, 152 and 214 days after spraying for analysis. A time series hydrogen stable isotope pro- file of the soil water revealed that piston flow, which is the domi­ nant flow mechanism in near saturated formation, was excellent. Several studies have also been carried out with oxygen and hy- drogen stable isotopes as tracers in dry and semi­arid areas (BARNERS & ALLISON, 1983; DE VRIES et al., 2000). In ag- riculture, soil at 1 m depth has been actively studied. However, studies on soil at far greater depths have rarely been undertaken (BHARATI et al., 2002). Many different isotope tracers are used around the world based on the purpose and intent of a study. One of these tracers is tritium, a radioactive isotope of hydrogen. Tritium used to be a good tracer for tracking water movement through the unsatu- Article history: Manuscript received December 28, 2017 Revised manuscript accepted May 28, 2018 Available online June 21, 2018 Keywords: soil water, oxygen isotope, unsatu- rated zone, recharge rate, infiltration time G eo lo gi a C ro at ic a Geologia Croatica 71/266 rated zone and determining groundwater age because of it abun- dance in the atmosphere. In the arid climate of Arizona, it was used to determine the mixing degree between shallow and deep groundwater (HARRIS, 2000). In the humid climate of Japan, it was used as a tracer to determine the recharge rate and infiltra- tion time (KAYANE et al., 1980; SHIMADA, 1988). However, a few studies pointed out that tritium cannot be solely relied on be- cause its concentration keeps on dropping year after year in the atmosphere (TSUJIMURA & TANAKA, 1998). Consequently, in later studies, oxygen and hydrogen isotopes were used together instead as tracers to determine recharge rates especially in Japan (YABUSAKI et al., 2011; KUDO et al., 2016). Both recharge rate and unsaturated zone infiltration velocity are important variables that provide insight into contaminant movement through the un- saturated zone. In this study, the study area as shown in Figure 1, the Kuma- moto region, is almost 100% dependent on groundwater for drinking purposes. However, the nitrate concentration has begun to build up in the water, raising concerns about groundwater con- tamination (HOSONO et al., 2013). The high nitrate buildup oc- curs at high elevation areas which have lots of agricultural ac- tivities and are the recharge zones for Kumamoto groundwater. It is therefore necessary to understand the infiltration mechanism in the unsaturated zone of these areas. Recently, unsaturated zone soil samples (down to 5 m depth) were collected at the slope of the western foot of Mt. Aso and the amount of recharge was es- timated using oxygen and hydrogen isotope ratios of the water extracted from the soil (KUDO et al., 2016). Research on the deep unsaturated zone (up to 15 m in depth) in Kumamoto using isotope tracers is still limited. The aim of this study is to augment the efforts in unsaturated zone studies in the Kumamoto region by trying to clarify the infiltration mecha- nism through estimation of the recharge amount and downward velocity of soil water using oxygen isotope ratios (water) in the recharge zone. 2. STUDY AREA The Kumamoto region is about 1041 km2 in area and bordered by the Chikushi­mountains to the North, the Mashiki­mountains to the South and the slope of the western foot of Mt. Aso to the East (Figure 1). There are three main rivers in the region; the Ki- kuchi, Shira and Midori Rivers which all flow into the Ariake Sea. The hydrogeological basement of the Kumamoto region con- sists of Mesozoic metamorphic and igneous rocks. The basement rocks are overlain by Quaternary pyroclastic flow deposits with high permeability (MIYOSHI et al., 2009). These deposits also cover the three major plateaus in the region which are the Kiku- chi and Takayubaru plateaus to the east and the Ueki plateau to the North (Figure 1). They have altitudes of approximately 100 m. The unsaturated zone of these plateaus has a thickness of about 30 m. New volcanic ash layers are widely distributed on the top soil. The soil profiles of cores taken from the various sites studied are shown in Figure 2. Soil types include sandy clay, clay sand, volcanic ash sand, volcanic ash clay, gravelly clay, non- welded tuff and gravel. There are variations in soil type among the cores. Groundwater in the Kumamoto region is recharged on the slope of Mt. Aso and around the plateaus, and flows from the northeastern part of the region to the southwest (TANIGUCHI et al., 2003). The aquifer formed by Quaternary pyroclastic flow deposits are divided into two main types by an aquiclude layer of lacustrine sediments; unconfined and confined aquifers (SHI- Figure 1. A map showing the Kumamoto region including sampling points. Red points show the drilling sites of the cores. The black lines and pink lines highlight the shallow groundwater table in the high-water season and the plateau areas. G eologia C roatica Okumura et al.: Evaluations of the downward velocity of soil water movement in the unsaturated zone in a groundwater recharge area ... 67 MADA, 2012). The land­cover is 31% farmland, 29% forest and 11% paddy. The plateaus, which are groundwater recharge areas are mainly used as farmland. Average annual precipitation and temperature of Kumamoto from 1985 to 2015 are 1986 mm and 16.9 ˚C, respectively. 3. SAMPLING AND METHODS In this study, 5 sampling sites were selected on the plateaus in the region (Figure 1). Each sampling site shows a different soil type, different fertilizer application method as well as treatment, dif- ferent crops cultivated and different drilling times as shown in Table 1 and Figure 2. Core samples were taken from the unsatu- rated zone of each site using an excavator without adding water (ECO­3V, YBM, Japan). The core was cut into 0.1 m samples and vacuum packed on- site to prevent evaporation of soil moisture before being taken to the laboratory for analysis. The 0.1 m fractions were split into two and each placed in a 100 cc sampling can. From one, soil wa- ter was centrifuged at pF 4.2 using centrifuge (MODEL SS­2200, SAKUMA, Japan) which spins for 2 hours. Although different for each depth, 2 to 20 ml of soil water was extracted. For the other sample, a three­phase meter that operates by Charles Boyle’s law was used to measure the total volume of the liquid and solid phases after weighing (HORITA, 1985). The gas phase content (air within the pores) was obtained by subtracting the li­ quid and solid phase volumes from the total volume of the can. Precipitation data used in this study was gathered at the Ku- mamoto University from Jan, 2005 to Jul, 2016. The data was acquired by sampling rainfall two to three times every month in a 2000 ml plastic bottle equipped with a funnel. A ping­pong ball was placed in the funnel to prevent evaporation. Samples were analyzed for hydrogen and oxygen isotope ratios. The results were converted to monthly data by evaluating the weighted ave­ rage for each month. Figure 2. Soil profiles of drilled cores of the various sites. Table 1. Details of sampling points. For the three-phase distribution, samples at 0.9 – 1.0 m, 5.0 – 5.1 m and 9.9 – 10.0 m are displayed. Details of all the water con- tent data of the cores are shown in Appendix Table A1.   Altitude(m) Cultivated crop type Drilling date Depth (m) Application status of fertilizers Three- phase distribution (%) Total soil water content (mm)   0.9–1.0 m 5.0–5.1 m 9.9–10.0 m 0–1.0 m 0–5.0 m 0–10 m S1 98 corn for feed and Italian ryegrass Nov-14 15 slurry and fertilizers gas 9 14 45 580 2689 5331liquid 64 53 31 solid 27 33 24 S2 67 corn for feed and Italian ryegrass Nov-14 14 slurry and fertilizers gas 29 1 25 501 2729 5036liquid 53 57 34 solid 18 42 41 C1 105 vegetable May-12 20 chemical fertilizers gas 26 18 18 523 2345 4994liquid 55 52 47 solid 19 30 35 C2 121 vegetable May-12 15 chemical fertilizers gas 27 17 16 540 3175 5729liquid 58 54 50 solid 15 29 34 C3 137 carrot Sep-15 10 manure and fertilizers gas 26 12 5 536 3203 6249liquid 62 64 51 solid 12 24 44 G eo lo gi a C ro at ic a Geologia Croatica 71/268 Hydrogen and oxygen isotope ratios were measured by mass spectrometer (Delta­V, Thermo Fisher Scientific, USA). In the mass spectrometer, the gas achieved equilibrium with the oxygen and hydrogen isotopes of the water samples that were introduced. The hydrogen and oxygen isotopes are expressed as relative dif- ferences (δ values) from Standard Mean Ocean Water in per mil (‰). The accuracy of the measured value was within ± 0.50‰ for δD and within ± 0.05‰ for δ18O. 4. RESULTS Plots of δD and δ18O for all precipitation and soil water samples are shown in Figure 3. The elevation effect on water isotopes was evaluated. The maximum elevation difference between the cores was calculated to be 70 m. This elevation effect on the hydrogen isotope in the study area is reported as -0.027‰ per metre (KAGABU et al., 2017). Hence, the maximum elevation effect of the sampling points is about 1.9‰. However, it can be seen from Figure 3 that all plots of δD and δ18O fall along the summer Lo- cal Meteoric Water Line (April to September) regardless of eleva- tion effect. Therefore, it was not considered in our estimations. The isotope ratios of precipitation for 11 years (2005 to 2015) were divided into two groups depending on season; summer (April to September) and winter (October to March). The slopes of the regression lines of the summer and winter data are 8.5 (r2 Figure 3. A plot diagram for δ18O against δD of soil water samples. Figure 4. Oxygen stable isotope ratio vertical profile diagrams for each core. Triangle marks show peak depth with a relatively high isotope ratio. G eologia C roatica Okumura et al.: Evaluations of the downward velocity of soil water movement in the unsaturated zone in a groundwater recharge area ... 69 = 0.87, p < 0.0001, n = 70) and 8.0 (r2 = 0.84, p < 0.0001, n = 65) respectively, which are almost equal to 8, the slope of the World Meteoric Water Line (CRAIG, 1961). However, the intercept of the regression line for summer and winter data are 12.8 and 19.2, respectively. The intercept for all soil water was 8.8 (r2 = 0.83, p < 0.01, n = 566) which was rela- tively close to the intercept for summer (Figure 3). Moreover, the averages of δD and δ18O of soil water samples were –41.3‰ and –6.7‰, respectively which are similar to the isotopic composition for summer precipitation (δD = –45‰, δ18O = –7‰) compared with that of winter (δ18O = –5‰, δD = –32‰). Evaporation oc- curring in the soil is generally considered to be non­equilibrium evaporation, in which case the slope of a regression line in the soil water tends to be smaller ranging from 2 to 5 (BARNES & TURNER, 1998; CLARK & FRITZ, 1997). In this study, the slope for all soil water sample plots was 8.1 (r2 = 0.83, p < 0.01, n = 566), which implies evaporation in the top soil was not consi- derable. Figure 4 shows the vertical profiles of δ18O in soil water. These profiles display several relatively high isotopic composi- tion peaks, e.g., at depths of 1.2 m and 3.5 m for the S1 core. It is interpreted that the vertical change of δ18O is reflective of the sea- sonal isotopic composition of the recharging precipitation which is high in summer and low in winter. These peaks hold the sea- sonal information of precipitation. The plots in Figure 4 show that it takes one year for new peaks to appear on the profile. It can be inferred from the S1 core profile that the infiltration rate in the top 3.5 m would be 2.2 m/yr approximately. The next peak after 3.5 m is at 10 m depth. There- fore, the depth interval from peak to peak is observed to be in- creasing. Moreover, there is a gradual change in peak compared with the peak at 3.5 m depth. The profiles of the other cores show similar characteristic peaks. It is assumed that as soil water infil- trates deeper, the more dispersion may occur when the peaks are averaged. Therefore, there is a limit to understanding the infiltra- tion rate from the peak position. Table 1 shows the liquid and solid phases at depths of 1 m, 5 m and 10 m for each core. In all cores, the solid phase varies be- tween 15% and 27% at 1 m depth, while porosity ranges between 73 and 88%. According to SHIMOZU (1986), Mt. Aso volcanic ash soil porosity ranges from approximately 70 to 90%. Hence, the sampling points have the characteristics of volcanic ash soil. The S1 liquid at 10 m depth is small compared with other cores. On the other hand, in C3, the liquid phase occupies 96% of the pore volume at a depth of 10 m. In particular, C3 has a high liq- uid phase at all depths. Therefore, C3 soil is considered to have a relatively high water holding capacity. It is important to deter- mine the recharge rate and downward velocity of soil water by incorporating a water content profile. 5. DISCUSSION In order to estimate the average downward velocity of soil water from 0–15 m depth using stable isotope ratios, the isotope profile of soil water was compared with the model isotope profile of the monthly infiltration amount obtained by subtracting evapotrans- piration from precipitation. In building the model profile based on precipitation, the time-series data of precipitation was con- verted into depth data. To do this, the Displacement Flow Model (DFM) proposed by ANDERSON & SEVEL (1974) was applied. DFM was used earlier by SHIMADA (1988) and KUDO et al. (2016) to understand the behaviour of water in the unsaturated zone. The model assumes a piston flow. Here, a piston flow is also assumed in an attempt to estimate the recharge rates and the downward velocity. The methods used to calculate DFM are described below. Equation (1) which is the water balance equation was used to es- timate Infiltration (I) into the ground. I = P-R-E (1) Where P, R and E are amounts of precipitation, runoff and evapo­ transpiration, respectively. In estimating E, Equation (2) was used. This is a modified form of Thornthwaite’s equation (THORNTHWAITE, 1948) used to handle wide temperature ranges. This is based on the principle that the amounts of precip- itation and evapotranspiration are directly proportional to the at- mospheric pressure (TAKAHASHI, 1979). 2 3100PE(T) = 34.4T3100 +1.8P exp(– ) 235 + T (2) Where T is monthly temperature, P is monthly precipitation. Here, R in equation (1) was replaced with αP by setting the direct runoff coefficient α, assuming that a constant rate of P di- rectly flows out. α was varied from 0 to 0.3 at an interval of 0.02 with reference to KUDO et al. (2016), and the highest coefficient of determination between the actual profile and the modeled pro- file was selected. The fraction of monthly precipitation used for each depth was determined to successively represent infiltration from the surface which corresponds to the soil water content. Based on the fraction of the monthly precipitation for each depth, weighted averages of the oxygen isotope ratios in precipitation were estimated to create a model isotope vertical profile (TSU- JIMURA et al., 1994). DFM was used to create a depth profile by applying the time variation of the tracer concentration. The downward velocity of soil water and recharge rate were estimated based on the depth­ time information obtained when the profile was created using DFM. Monthly temperature and precipitation data for Kumamoto City collected by the Japan Meteorological Agency were used in the DFM. Time series data used in the DFM calculations are shown in Figure 5 and include precipitation, evapotranspiration, temperature and δ18O in precipitation. The profile of δ18O in soil water and that of the modeled pro- file by DFM are shown in Figure 6. The coefficient of determina- tion (r2) between the measured δ18O and modeled δ18O by DFM was lower than 0.5 for all cores (black line vs gray line in Figure 6). This indicates that direct results by DFM could not trace the behaviour of measured δ18O profile successfully. This may be due to the fact that input precipitation δ18O data are based on a weighted average of several precipitation events and did not cover precisely all actual precipitation δ18O records. Moreover, the con- cept of the DFM model might be the other reason which does not account for dispersion phenomena. To solve this problem, vari- ance due to these factors was considered by calculating moving averages of DFM values and the condition that resulted in the highest correlation between measured δ18O and modeled δ18O was employed (KUDO et al., 2016). Consequently, we found the best condition resulting in the highest correlation between mea­ sured δ18O and modeled δ18O (moving average DFM), as shown by the black and dotted lines in Figure 6. The coefficient of de- termination for all cores was (r2> 0.8, p <0.02), suggesting that G eo lo gi a C ro at ic a Geologia Croatica 71/270 Figure 5. Time series distribution of (a) Precipitation (b) Temperature (c) Evapotranspiration (d) Oxygen isotope ratio in precipitation (e) Monthly average of pre- cipitation (bar graph) and oxygen isotope ratio (line graph) from 2005 to 2015. The dotted lines in (a) and (d) represent the moving average of 3 month data. The hatched area in (d) represents the summer season (April – September). Table 2. Infiltration time and velocity of studied cores estimated using DFM. The thickness of the unsaturated zone is estimated using shallow groundwater level distribution. S1 S2 C1 C2 C3 1058 846 745 795 869 2.34 1.68 1.46 1.38 1.37 30 15 33 33 19 13 9 23 24 14Average water transportation time from surface reaching to aquifer (yr) Annual average of recharge rates (mm/yr) Annual average of downward velocity (m/yr) Thickness of unsaturated layer (m) G eologia C roatica Okumura et al.: Evaluations of the downward velocity of soil water movement in the unsaturated zone in a groundwater recharge area ... 71 our DFM approach satisfactorily reflects water behaviour at the studied sites. The estimated result for each site is shown in Table 2. In S1, it was observed that the downward velocity was the highest of all the sites. This is because the soil has a low liquid phase around 10 m depth. Comparing C3 and S1 which have the same soil type, S1 has a higher recharge rate and velocity. This may be due to the difference in soil conditions. For C3 and S2, it can be seen that the downward velocity of C3 is relatively lower, even though the recharge rate is higher. The most likely reason is that, C3 soil has the highest water content (Table 1). Therefore, it is evident that the difference in the average recharge rate and downward velo­ city for each core is due to the difference in soil conditions such as soil type and water content at each core depth (Table 1 and Figure 2). Although there are regional differences, the annual average recharge rate in the recharge area of the plateau was estimated to range from 745 to 1058 mm/yr, and the annual average downward velocity from 1.37 to 2.34 m/yr. Furthermore, the average re- charge rate and average downward velocity calculated from the estimation results in Table 2 for S1, C2 and C3 in the northeast- ern recharge area (Figure 1) are 893 mm/yr and 1.7 m/yr, respec- tively. These somehow match the recharge amount of 1137 mm/ yr and infiltration rate of 2.3 m/yr of the Kumamoto region esti- mated using tritium (SHIMADA & UENO, 2016). However, our estimated value was smaller than that of SHIMADA & UENO (2016). The difference may be due to regional heterogeneities. In estimating the infiltration time for water to reach the aq- uifers, the unsaturated zone thickness was divided by the down- ward velocity as shown in Table 2. The unsaturated zone thick- ness was obtained by subtracting the groundwater level elevation in the lowest water level period at the sampling points from the ground surface elevation. The transportation time from the ground surface to the aquifer was estimated to range from 9 to 24 years. KAGABU et al. (2017) estimated the ages of ground- water in the recharge zone at Kikuchi plateau using 85Kr age tracer to range from 15 to 25 years (n = 3). Although different sample points were selected in this study, the water transporta- tion time from the surface to the aquifer estimated by DFM is equivalent to the recharge area’s groundwater ages calculated by KAGABU et al. (2017). Therefore, it can be reliably concluded that soil water reaches the aquifer over a period of about 9 to 25 years in the main recharge area of the Kumamoto region. 6. CONCLUSION The recharge rate and downward velocity in the unsaturated zone of the recharge area of the Kumamoto region were estimated for 5 soil cores using oxygen isotope ratios in soil water as a tracer. Consequently, the annual average recharge rate was estimated to range from 745 to 1058 mm/yr, and the annual average downward velocity from 1.37 to 2.34 m/yr. Differences in the estimated re- charge rate and downward movement velocity are due to the vari- ation in soil properties of each site. Water transportation time from the surface to the aquifers was estimated to be 9 to 24 years, corresponding well to groundwater ages in the same recharge area. With the assumption that nitrogen loaded on the surface will be transported with soil water, nitrate should leach to the aquifer in 9 to 24 years once fertilizers and manures are applied. Such information is primarily important for the management and pre- servation of groundwater resources. However, nitrate transporta- tion and behaviour in the unsaturated zone should be affected by diffusion, microbial activities, etc. The results of this study there- fore may not be able to fully account for the transportation of so­ lutes through the unsaturated zone to the aquifers. To better un- derstand nitrate infiltration characteristics, it is necessary to promote future studies on nitrate concentrations and isotope ra- tios to aid further understanding of soil water infiltration mecha- nisms. ACKNOWLEDGMENT We thank Mr. Satoshi SAKAEDA of the Kumamoto Prefectural Government for his help during the field surveys. 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Land Use Control back­ up System, Retrieved from http://lucky.tochi.mlit.go.jp/ JAPAN METEOROLOGICAL AGENCY (March 20, 2018), Past climate data, Re- trieved from http://www.data.jma.go.jp/gmd/risk/obsdl/index.php G eologia C roatica Okumura et al.: Evaluations of the downward velocity of soil water movement in the unsaturated zone in a groundwater recharge area ... 73 APPENDIX Table A1 Isotope composition of soil water in each core. depth (m) δD (‰) δ18O (‰) d-excess (‰) δD (‰) δ18O (‰) d-excess (‰) δD (‰) δ18O (‰) d-excess (‰) 0.0 - 0.1 -42.1 -7.13 14.94 -23.5 -4.18 9.95 -64.1 -8.84 6.61 0.1- 0.2 -27.9 -4.93 11.54 -25.8 -4.57 10.79 -72.8 -10.35 10.07 0.2 - 0.3 -36.3 -5.71 9.38 -33.6 -5.08 7.03 -56.2 -8.34 10.53 0.3 - 0.4 -42.2 -6.55 10.20 -38.7 -5.69 6.87 -44.3 -6.66 9.00 0.4 - 0.5 -45.3 -6.84 9.42 -41.2 -5.91 6.11 -42.8 -6.09 5.91 0.5 - 0.6 -50.0 -7.27 8.16 -45.82 -6.16 3.43 -45.8 -6.35 5.03 0.6 - 0.7 -56.5 -7.94 7.02 -50.2 -6.77 3.99 -47.4 -6.48 4.43 0.7 - 0.8 -56.7 -7.97 7.06 -55.2 -7.36 3.69 -48.7 -6.90 6.46 0.8 - 0.9 -54.1 -7.67 7.26 -59.9 -7.88 3.15 -47.3 -6.84 7.36 0.9 - 1.0 -50.8 -7.24 7.12 -61.0 -7.97 2.77 -45.0 -6.64 8.11 1.0 - 1.1 -47.0 -6.76 7.08 -59.0 -7.82 3.53 -41.9 -6.29 8.34 1.1 - 1.2 -46.4 -6.61 6.48 -52.1 -6.95 3.51 -70.5 -7.09 -13.80 1.2 - 1.3 -45.9 -6.63 7.14 -41.1 -5.77 5.04 -39.1 -6.07 9.45 1.3 - 1.4 -46.6 -6.76 7.48 -33.6 -5.12 7.34 -33.8 -5.40 9.45 1.4 - 1.5 -48.1 -6.92 7.26 -50.3 -7.39 8.87 -29.5 -4.87 9.45 1.5 -1.6 -49.4 -7.16 7.88 -44.5 -6.54 7.84 -29.5 -4.76 8.55 1.6 - 1.7 -53.0 -7.48 6.84 -36.7 -6.13 12.28 -31.0 -4.80 7.36 1.7 - 1.8 -53.6 -7.59 7.12 -38.1 -6.22 11.65 -33.9 -5.09 6.80 1.8 - 1.9 -54.1 -7.75 7.90 -42.1 -6.19 7.43 -35.3 -5.38 7.75 1.9 - 2.0 -53.8 -7.74 8.12 -44.5 -5.95 3.12 -38.6 -5.86 8.25 2.0 - 2.1 -52.8 -7.74 9.12 -44.5 -6.24 5.37 -41.5 -6.12 7.47 2.1 - 2.2 -52.1 -7.69 9.42 -43.1 -6.13 5.92 -43.3 -6.32 7.23 2.2 - 2.3 -50.8 -7.62 10.16 -43.4 -6.06 5.01 -43.2 -6.34 7.49 2.3 - 2.4 -48.7 -7.44 10.82 -43.9 -6.03 4.28 -44.2 -6.47 7.54 2.4 - 2.5 -47.5 -7.40 11.70 -43.8 -6.08 4.82 -43.6 -6.38 7.42 2.5 - 2.6 -46.5 -7.27 11.66 -43.5 -6.05 4.97 -43.9 -6.44 7.56 2.6 - 2.7 -44.8 -7.15 12.40 -43.7 -6.00 4.33 -44.2 -6.42 7.17 2.7 - 2.8 -43.3 -6.94 12.22 -43.3 -6.06 5.14 -44.8 -6.45 6.80 2.8 - 2.9 -41.8 -6.81 12.68 -43.2 -5.90 4.06 -44.6 -6.44 6.90 2.9 - 3.0 -41.7 -6.60 11.10 -44.0 -5.93 3.48 -44.7 -6.38 6.37 3.0 - 3.1 -41.3 -6.67 12.06 -46.8 -6.23 3.05 -45.6 -6.64 7.51 3.1 - 3.2 -40.6 -6.68 12.84 -48.3 -6.42 3.05 -45.8 -6.61 7.16 3.2 - 3.3 -40.3 -6.51 11.78 -49.6 -6.50 2.42 -46.7 -6.74 7.17 3.3 - 3.4 -40.8 -6.61 12.08 -51.7 -6.69 1.89 -47.0 -6.82 7.61 3.4 - 3.5 -43.5 -6.15 5.70 -52.9 -6.91 2.40 -48.0 -6.89 7.10 3.5 - 3.6 -44.8 -6.22 4.96 -52.4 -6.97 3.30 -48.4 -6.96 7.30 3.6 - 3.7 -46.4 -6.48 5.44 -51.9 -7.20 5.63 -47.2 -6.78 7.05 3.7 - 3.8 -47.5 -6.52 4.66 -54.3 -7.14 2.77 -48.4 -6.81 6.07 3.8 - 3.9 -47.9 -6.53 4.34 -56.7 -7.62 4.22 -49.0 -6.93 6.43 3.9 - 4.0 -49.0 -6.74 4.92 -57.8 -7.76 4.26 -49.4 -6.97 6.34 4.0 - 4.1 -49.3 -6.77 4.86 -60.0 -8.03 4.30 -50.8 -7.09 5.88 4.1 - 4.2 -49.6 -6.92 5.76 -60.3 -8.19 5.27 -51.9 -7.20 5.68 4.2 - 4.3 -49.9 -7.03 6.34 -61.3 -8.22 4.47 -52.3 -7.15 4.91 4.3 - 4.4 -50.0 -7.06 6.48 -60.8 -8.24 5.06 -52.5 -7.21 5.17 4.4 - 4.5 -50.0 -7.06 6.48 -60.6 -8.14 4.48 -52.8 -7.23 5.00 4.5 - 4.6 -50.4 -7.15 6.80 -59.7 -8.00 4.28 -51.7 -6.99 4.21 4.6 - 4.7 -51.6 -7.37 7.36 -59.9 -8.09 4.84 -53.1 -7.29 5.19 4.7 - 4.8 -52.5 -7.56 7.98 -60.2 -8.11 4.71 -52.7 -7.18 4.77 4.8 - 4.9 -53.8 -7.83 8.84 -58.4 -7.83 4.26 -53.2 -7.35 5.64 4.9 - 5.0 -54.9 -7.96 8.78 -56.7 -7.67 4.69 -53.20 -7.39 5.95 5.0 - 5.1 -57.2 -8.18 8.24 -57.6 -7.96 6.08 -53.2 -7.44 6.27 5.1 - 5.2 -58.1 -8.46 9.58 -57.7 -7.92 5.58 -53.6 -7.42 5.74 5.2 - 5.3 -58.6 -8.40 8.60 -57.6 -7.84 5.10 -53.2 -7.47 6.48 5.3 - 5.4 -58.9 -8.50 9.10 -53.8 -7.60 7.01 -53.2 -7.45 6.38 5.4 - 5.5 -58.5 -8.44 9.02 -53.9 -7.60 6.90 -53.3 -7.49 6.66 5.5 - 5.6 -58.8 -8.40 8.40 -53.0 -7.43 6.45 -52.5 -7.27 5.67 5.6 - 5.7 -58.2 -8.38 8.84 -53.3 -7.42 6.07 -52.9 -7.31 5.57 5.7 - 5.8 -58.1 -8.37 8.86 -52.8 -7.37 6.15 -52.8 -7.28 5.43 5.8 - 5.9 -58.1 -8.36 8.78 -52.2 -7.25 5.77 -53.0 -7.26 5.09 5.9 - 6.0 -58.1 -8.36 8.78 -51.5 -7.21 6.11 -52.9 -7.18 4.52 6.0 - 6.1 -57.4 -8.28 8.84 -49.8 -6.97 5.99 -52.3 -7.13 4.71 6.1 - 6.2 -57.4 -8.23 8.44 -50.0 -6.99 5.96 -52.6 -7.16 4.66 6.2 - 6.3 -57.0 -8.19 8.52 -49.3 -6.86 5.65 -52.7 -7.15 4.46 6.3 - 6.4 -56.1 -8.03 8.14 -49.2 -6.88 5.86 -53.3 -7.21 4.33 6.4 - 6.5 -57.0 -8.11 7.88 -48.9 -6.84 5.85 -53.2 -7.21 4.47 6.5 - 6.6 -57.0 -8.18 8.44 -49.2 -6.89 5.96 -52.8 -7.23 5.03 6.6 - 6.7 -55.8 -8.00 8.20 -48.2 -6.68 5.27 -52.2 -7.11 4.71 6.7 - 6.8 -55.5 -7.94 8.02 -48.6 -6.82 5.97 -48.6 -6.84 6.05 6.8 - 6.9 -55.5 -7.89 7.62 -47.4 -6.64 5.75 -45.8 -6.44 5.80 6.9 - 7.0 -54.0 -7.75 8.00 -47.4 -6.62 5.64 -43.5 -6.17 5.82 S2 core C3 coreS1 core G eo lo gi a C ro at ic a Geologia Croatica 71/274 depth (cm) δD (‰) δ18O (‰) d-excess (‰) δD (‰) δ18O (‰) d-excess (‰) δD (‰) δ18O (‰) d-excess (‰) 7.0 - 7.1 -50.7 -7.62 10.26 -44.5 -6.47 7.30 -43.6 -6.07 4.99 7.1 - 7.2 -50.3 -7.58 10.34 -44.1 -6.56 8.36 -43.5 -6.09 5.21 7.2 - 7.3 -49.8 -7.6 11.00 -43.4 -6.44 8.03 -43.7 -5.97 4.06 7.3 - 7.4 -49.6 -7.49 10.32 -44.0 -6.50 7.98 -43.9 -6.31 6.59 7.4 - 7.5 -48.5 -7.43 10.94 -43.8 -6.44 7.77 -45.2 -6.25 4.78 7.5 - 7.6 -48.3 -7.35 10.50 -44.2 -6.51 7.94 -44.0 -6.31 6.48 7.6 - 7.7 -46.9 -7.27 11.26 -44.9 -6.59 7.83 -44.1 -6.35 6.69 7.7 - 7.8 -46.6 -7.21 11.08 -44.5 -6.49 7.47 -43.3 -6.20 6.30 7.8 - 7.9 -45 -6.98 10.84 -43.6 -6.40 7.55 -43.8 -6.33 6.90 7.9 - 8.0 -45.2 -7 10.80 -42.7 -6.13 6.29 -42.8 -6.12 6.21 8.0 - 8.1 -44.6 -6.86 10.28 -44.8 -6.52 7.39 -44.7 -6.45 6.90 8.1 - 8.2 -42.7 -6.81 11.78 -44.8 -6.48 7.09 -43.4 -6.24 6.47 8.2 - 8.3 -42.3 -6.71 11.38 -45.5 -6.66 7.73 -44.0 -6.33 6.64 8.3 - 8.4 -42 -6.64 11.12 -45.1 -6.67 8.25 -43.9 -6.36 6.95 8.4 - 8.5 -40.9 -6.59 11.82 -44.5 -6.53 7.72 -43.4 -6.26 6.64 8.5 - 8.6 -40.4 -6.48 11.44 -45.4 -6.59 7.39 -43.0 -6.40 8.24 8.6 - 8.7 -40.1 -6.45 11.50 -45.1 -6.54 7.26 -42.6 -6.43 8.86 8.7 - 8.8 -39.9 -5.26 2.18 -43.8 -6.17 5.58 -42.1 -6.45 9.50 8.8 - 8.9 -38.5 -6.31 11.98 -43.1 -6.10 5.69 -42.5 -6.36 8.40 8.9 - 9.0 -37.7 -6.24 12.22 -43.0 -6.23 6.86 -42.4 -6.33 8.21 9.0 - 9.1 -37.9 -6.18 11.54 -43.5 -6.27 6.67 -44.6 -6.61 8.28 9.1 - 9.2 -37.7 -6.21 11.98 -44.1 -6.45 7.51 -44.1 -6.49 7.82 9.2 - 9.3 -37.3 -6.08 11.34 -44.0 -6.41 7.29 -43.1 -6.46 8.54 9.3 - 9.4 -37.3 -6.14 11.82 -44.2 -6.42 7.12 -41.9 -6.20 7.72 9.4 - 9.5 -37.7 -6.08 10.94 -43.6 -6.30 6.76 -41.3 -6.17 8.08 9.5 - 9.6 -37.5 -6.02 10.66 -43.7 -6.40 7.54 -40.5 -6.14 8.63 9.6 - 9.7 -37.4 -6.01 10.68 -42.3 -6.05 6.08 -41.0 -6.16 8.34 9.7 - 9.8 -37 -5.94 10.52 -42.7 -6.09 6.07 -39.9 -6.04 8.44 9.8 - 9.9 -37.7 -6.04 10.62 n.d. n.d. n.d. -40.7 -6.02 7.47 9.9 - 10.0 -35.9 -5.67 9.46 -39.1 -5.32 3.53 -42.9 -6.41 8.33 10.0 - 10.1 -34.4 -5.21 7.28 -43.9 -6.28 6.38 -47.1 -6.81 7.41 10.1 - 10.2 -36.8 -5.68 8.64 -43.0 -6.36 7.86 10.2 - 10.3 -37.4 -5.84 9.32 -43.1 -6.34 7.64 10.3 - 10.4 -37.4 -5.79 8.92 -43.4 -6.44 8.06 10.4 - 10.5 -37.9 -5.14 3.22 -42.6 -6.41 8.68 10.5 - 10.6 -37.6 -6.08 11.04 -43.5 -6.34 7.24 10.6 - 10.7 -38.2 -6.76 15.88 -43.0 -6.46 8.68 10.7 - 10.8 -39 -6.82 15.56 -43.0 -6.32 7.59 10.8 - 1.09 -39.1 -6.8 15.30 -41.5 -6.13 7.59 10.9 - 11.0 -37.8 -6.49 14.12 -41.7 -6.09 7.02 11.0 - 11.1 -39.5 -6.7 14.10 -42.7 -6.30 7.71 11.1 - 11.2 -40.3 -6.82 14.26 -42.9 -6.37 8.00 11.2 - 11.3 -40.6 -6.64 12.52 -43.5 -6.40 7.76 11.3 - 11.4 -41.3 -6.68 12.14 -43.3 -6.36 7.60 11.4 - 11.5 -42.2 -6.76 11.88 -43.1 -6.32 7.53 11.5 - 11.6 -42.5 -6.73 11.34 -43.1 -6.30 7.36 11.6 - 11.7 -42.1 -6.65 11.10 -42.7 -6.17 6.73 11.7 - 11.8 -42.6 -6.64 10.52 -43.0 -6.18 6.45 11.8 - 11.9 -43.3 -6.67 10.06 -42.8 -6.11 6.01 11.9 - 12.0 -42.9 -6.48 8.94 -43.3 -6.15 5.95 12.0 - 12.1 -44 -6.63 9.04 -44.4 -6.51 7.63 12.1 - 12.2 -44.2 -6.6 8.60 -44.1 -6.47 7.70 12.2 - 12.3 -44.2 -6.86 10.68 -44.6 -6.53 7.64 12.3 - 12.4 -45 -6.93 10.44 -44.7 -6.59 8.07 12.4 - 12.5 -43.5 -6.36 7.38 -44.2 -6.54 8.13 12.5 - 12.6 -43.4 -6.38 7.64 -42.9 -6.53 9.29 12.6 - 12.7 -45.0 -6.46 6.68 -43.5 -6.42 7.90 12.7 - 12.8 -44.9 -6.53 7.34 -43.9 -6.48 7.97 12.8 - 12.9 -45.7 -6.75 8.30 -43.7 -6.41 7.60 12. 9 -13.0 -43.9 -6.49 8.02 -42.9 -6.22 6.84 13.0 - 13.1 -45.7 -6.91 9.58 -43.2 -6.28 7.02 13.1 - 13.2 -46.1 -7.00 9.90 -42.9 -6.34 7.79 13.2 - 13.3 -46.1 -7.06 10.38 -42.1 -6.23 7.74 13.3 - 13.4 -45.7 -7.08 10.94 -41.2 -6.14 7.98 13.4 - 13.5 -46.2 -7.10 10.60 -41.1 -6.06 7.38 13.5 - 13.6 -46.3 -7.08 10.34 -40.2 -5.86 6.71 13.6 - 13.7 -46.4 -7.07 10.16 -40.7 -5.95 6.95 13.7 - 13.8 -46.3 -6.92 9.06 -40.2 -5.91 7.12 13.8 - 13.9 -45.1 -6.93 10.34 -39.3 -5.79 7.03 13.9 - 14.0 -45.1 -6.97 10.66 -39.6 -5.84 7.10 14.0 - 14.1 -44.9 -6.97 10.86 14.1 - 14.2 -45.7 -7.08 10.94 14.2 - 14.3 -45.8 -6.47 5.96 14.3 - 14.4 -45.1 -6.37 5.86 14.4 - 14.5 -44.9 -6.29 5.42 14.5 - 14.6 -44.8 -6.45 6.80 14.6 - 14.7 -44.6 -6.60 8.20 14.7 - 14.8 -44.4 -6.64 8.72 14.8 - 14.9 -44.4 -6.31 6.08 14.9 - 15.0 -43.5 -6.11 5.38 S1 core S2 core C3 core Table A1. Continuation. G eologia C roatica Okumura et al.: Evaluations of the downward velocity of soil water movement in the unsaturated zone in a groundwater recharge area ... 75 depth (m) δD (‰) δ18O (‰) d-excess (‰) δD (‰) δ18O (‰) d-excess (‰) 0.0 - 0.2 -25.4 -3.01 -1.28 -26.3 -4.64 10.84 0.2 - 0.4 -24.8 -3.85 6.00 -26.7 -4.87 12.32 0.4 - 0.6 -28.0 -4.65 9.19 -33.8 -5.32 8.68 0.6 - 0.8 -30.1 -4.67 7.31 -41.4 -6.11 7.45 0.8 - 1.0 -39.3 -5.23 2.59 -50.6 -6.93 4.81 1.0 - 1.2 -55.7 -7.09 0.98 -36.3 -5.60 8.56 1.2 - 1.4 -61.1 -7.82 1.50 -29.6 -4.01 2.51 1.4 - 1.6 -59.8 -7.68 1.68 -58.9 -8.08 5.72 1.6 - 1.8 -50.9 -6.52 1.25 -57.2 -8.00 6.79 1.8 - 2.0 -36.5 -5.13 4.48 -51.4 -7.35 7.39 2.0 - 2.2 -40.6 -5.45 2.99 -44.7 -6.41 6.60 2.2 - 2.4 -38.5 -5.14 2.61 -43.1 -6.27 7.08 2.4 - 2.6 -36.1 -4.80 2.31 -40.2 -5.93 7.23 2.6 - 2.8 -65.7 -5.04 4.64 -37.9 -5.68 7.49 2.8 - 3.0 -32.7 -4.57 3.86 -36.4 -5.49 7.51 3.0 - 3.2 -32.5 -4.92 6.92 -35.2 -5.36 7.62 3.2 - 3.4 -29.6 -4.34 5.14 -34.9 -5.28 7.33 3.4 - 3.6 -29.8 -4.37 5.17 -35.6 -5.29 6.70 3.6 - 3.8 -30.0 -4.16 3.24 -36.6 -5.39 6.45 3.8 - 4.0 -32.2 -4.39 2.94 -39.3 -5.66 5.98 4.0 - 4.2 -35.9 -5.00 4.11 -41.5 -6.04 6.79 4.2 -4.4 -39.3 -5.48 4.59 -42.7 -6.15 6.44 4.4 - 4.6 -42.1 -5.81 4.38 -44.1 -6.34 6.55 4.6 - 4.8 -43.1 -5.81 3.38 -45.7 -6.52 6.44 4.8 - 5.0 -48.7 -6.58 3.99 -47.1 -6.67 6.28 5.0 - 5.2 -50.9 -6.88 4.11 -48.3 -6.84 6.42 5.2 - 5.4 -48.2 -6.39 2.90 -48.0 -6.91 7.25 5.4 - 5.6 -48.9 -6.71 4.73 -47.8 -6.87 7.08 5.6 - 5.8 -46.9 -6.44 4.59 -46.8 -6.80 7.61 5.8 - 6.0 -44.6 -6.20 4.98 -44.9 -6.50 7.11 6.0 - 6.2 -38.3 -5.28 3.92 -43.2 -6.28 7.10 6.2 - 6.4 -43.6 -6.34 7.14 -41.9 -6.19 7.65 6.4 - 6.6 -42.2 -5.96 5.49 -41.0 -6.06 7.52 6.6 - 6.8 -41.3 -5.87 5.67 -39.9 -5.85 6.92 6.8 - 7.0 -39.9 -5.58 4.72 -38.7 -5.75 7.27 7.0 - 7.2 -38.8 -5.19 2.76 -39.6 -5.92 7.73 7.2 - 7.4 -38.0 -5.13 3.05 -39.0 -5.73 6.87 7.4 - 7.6 -38.4 -5.19 3.16 -38.8 -5.72 7.00 7.6 - 7.8 -37.8 -5.18 3.63 -38.0 -5.54 6.35 7.8 - 8.0 -36.0 -4.86 2.90 -36.9 -5.39 6.26 8.0 - 8.2 -36.6 -4.92 2.74 -37.7 -5.56 6.80 8.2 - 8.4 -34.9 -4.72 2.88 -37.5 -5.65 7.64 8.4 - 8.6 -35.3 -4.78 2.94 -37.1 -5.57 7.42 8.6 - 8.8 -34.6 -4.93 4.85 -37.0 -5.55 7.41 8.8 - 9.0 -33.7 -4.80 4.75 -36.7 -5.49 7.23 9.0 - 9.2 -30.9 -4.22 2.86 -36.2 -5.43 7.18 9.2 - 9.4 -30.2 -4.29 4.07 -36.3 -5.48 7.54 9.4 - 9.6 -30.5 -4.38 4.53 -36.0 -5.37 6.99 9.6 - 9.8 -30.3 -4.40 4.98 -35.8 -5.30 6.53 9.8 - 10.0 -29.2 -4.02 2.94 -34.9 -5.15 6.32 C1 C2 Table A1. Continuation. G eo lo gi a C ro at ic a Geologia Croatica 71/276 depth(cm) δD (‰) δ18O (‰) d-excess (‰) δD (‰) δ18O (‰) d-excess (‰) 10.0 - 10.2 -27.5 -3.59 1.21 -35.1 -5.28 7.09 10.2 - 10.4 -24.7 -2.65 -3.51 -35.0 -5.30 7.45 10.4 - 10.6 -22.5 -2.20 -4.85 -35.0 -5.21 6.69 10.6 - 10.8 -23.9 -2.55 -3.55 -34.7 -5.19 6.84 10.8 - 11.0 -24.4 -2.69 -2.91 -34.0 -5.21 7.62 11.0 - 11.2 -28.0 -3.70 1.65 -35.2 -5.19 6.35 11.2 - 11.4 -27.5 -3.49 0.42 -34.2 -4.93 5.30 11.4 - 11.6 -26.3 -3.30 0.08 -33.6 -5.03 6.66 11.6 - 11.8 -29.1 -3.90 2.06 -32.9 -4.96 6.73 11.8 - 12.0 -26.1 -3.17 -0.75 -32.7 -4.69 4.80 12.0 - 12.2 -25.6 -3.14 -0.51 -33.0 -4.78 5.19 12.2 - 12.4 -27.1 -3.51 0.91 -32.5 -4.76 5.55 12.4 - 12.6 -25.8 -3.17 -0.44 -32.3 -4.70 5.32 12.6 - 12.8 -25.8 -3.12 -0.80 -32.5 -4.65 4.76 12.8 - 13.0 -26.3 -3.37 0.66 -30.4 -4.35 4.47 13.0 - 13.2 -24.0 -2.79 -1.60 -32.5 -4.55 3.93 13.2 - 13.4 -26.3 -3.49 1.61 -32.6 -4.65 4.58 13.4 - 13.6 -27.7 -3.84 2.99 -31.3 -4.56 5.15 13.6 - 13.8 -26.8 -3.63 2.28 -28.7 -3.72 1.06 13.8 - 14.0 -25.9 -3.38 1.13 -25.8 -3.24 0.04 14.0 - 14.2 -24.2 -2.89 -1.06 -27.0 -3.59 1.73 14.2 - 14.4 -24.8 -3.18 0.68 -23.7 -2.61 -2.79 14.4 - 14.6 -24.8 -3.13 0.22 -28.6 -3.89 2.51 14.6 - 14.8 -24.4 -3.06 0.11 -21.6 -2.13 -4.54 14.8 - 15.0 -20.5 -2.07 -3.97 -16.1 -1.16 -6.88 15.0 - 15.2 -22.7 -2.61 -1.79 15.2 - 15.4 -25.7 -3.38 1.34 15.4 - 15.6 -22.7 -2.52 -2.60 15.6 - 15.8 -25.0 -3.18 0.41 15.8 - 16.0 -20.9 -2.16 -3.56 16.0 - 16.2 -24.1 -2.93 -0.63 16.2 - 16.4 -24.4 -2.99 -0.42 16.4 - 16.6 -24.5 -3.11 0.34 16.6 - 16.8 -27.3 -3.67 2.03 16.8 - 17.0 -26.3 -3.32 0.27 17.0 - 17.2 -29.3 -3.99 2.62 17.2 - 17.4 -29.2 -3.89 1.87 18.4 - 17.6 -32.7 -4.47 3.02 17.6 - 17.8 -34.5 -4.73 3.32 17.8 - 18.0 -34.3 -4.46 1.41 18.0 - 18.2 -31.0 -3.67 -1.71 18.2 - 18.4 -34.6 -4.54 1.66 18.4 - 18.6 -37.5 -5.01 2.54 18.6 - 18.8 -38.2 -5.05 2.21 18.8 - 19.0 -38.9 -5.12 2.04 19.0 - 19.2 -40.2 -5.46 3.43 19.2 - 19.4 -39.7 -5.36 3.18 19.4 - 19.6 -39.5 -5.19 2.06 19.6 - 19.8 -39.7 -5.15 1.44 19.8 - 20.0 -35.4 -4.34 -0.61 C1 C2 Table A1. Continuation. G eologia C roatica Okumura et al.: Evaluations of the downward velocity of soil water movement in the unsaturated zone in a groundwater recharge area ... 77 Gas phase Liquid phase Solid phase Gas phase Liquid phase Solid phase 0.0 - 0.1 53 9.3 52 38.7 7.0 - 7.1 58 2.5 57 40.5 0.1- 0.2 54 11.1 53 35.9 7.1 - 7.2 58 4.6 57 38.4 0.2 - 0.3 51 14.9 50 35.1 7.2 - 7.3 58 6.9 57 36.1 0.3 - 0.4 55 16 54 30 7.3 - 7.4 50 3.7 49 47.3 0.4 - 0.5 60 15 59 26 7.4 - 7.5 53 2.2 52 45.8 0.5 - 0.6 57 18.1 56 25.9 7.5 - 7.6 56 1.4 55 43.6 0.6 - 0.7 65 13 64 23 7.6 - 7.7 55 9.9 54 36.1 0.7 - 0.8 64 9.9 63 27.1 7.7 - 7.8 55 1.6 54 44.4 0.8 - 0.9 59 15.5 58 26.5 7.8 - 7.9 47 8.9 46 45.1 0.9 - 1.0 61 13.5 60 26.5 7.9 - 8.0 52 17.6 51 31.4 1.0 - 1.1 65 8.7 64 27.3 8.0 - 8.1 59 6 58 36 1.1 - 1.2 61 21.8 60 18.2 8.1 - 8.2 55 9.9 54 36.1 1.2 - 1.3 64 9 63 28 8.2 - 8.3 60 7.9 59 33.1 1.3 - 1.4 61 11.8 60 28.2 8.3 - 8.4 50 6 49 45 1.4 - 1.5 59 17.8 58 24.2 8.4 - 8.5 55 4.4 54 41.6 1.5 -1.6 49 12.6 48 39.4 8.5 - 8.6 43 7.2 42 50.8 1.6 - 1.7 52 19.2 51 29.8 8.6 - 8.7 56 7.4 55 37.6 1.7 - 1.8 51 19.9 50 30.1 8.7 - 8.8 59 3.4 58 38.6 1.8 - 1.9 51 11 50 39 8.8 - 8.9 55 11 54 35 1.9 - 2.0 46 27.9 45 27.1 8.9 - 9.0 57 3.5 56 40.5 2.0 - 2.1 57 27.5 56 16.5 9.0 - 9.1 51 17.9 50 32.1 2.1 - 2.2 61 11.8 60 28.2 9.1 - 9.2 45 20 44 36 2.2 - 2.3 59 27 58 15 9.2 - 9.3 41 28.8 44 27.2 2.3 - 2.4 60 18.8 59 22.2 9.3 - 9.4 38 36.5 37 26.5 2.4 - 2.5 54 21.9 53 25.1 9.4 - 9.5 34 35.3 34 30.7 2.5 - 2.6 57 19.5 56 24.5 9.5 - 9.6 30 44.7 29 26.3 2.6 - 2.7 53 11.9 52 36.1 9.6 - 9.7 32 20.7 35 44.3 2.7 - 2.8 62 14.75 61 24.25 9.7 - 9.8 34 32.1 33 34.9 2.8 - 2.9 51 26.2 50 23.8 9.8 - 9.9 33 20.9 38 41.1 2.9 - 3.0 48 13.8 47 39.2 9.9 - 10.0 32 45.1 31 23.9 3.0 - 3.1 46 21 45 34 10.0 - 10.1 33 n.d. n.d. n.d. 3.1 - 3.2 45 21.3 44 34.7 10.1 - 10.2 32 n.d. n.d. n.d. 3.2 - 3.3 45 21.6 44 34.4 10.2 - 10.3 32 47.5 32 20.5 3.3 - 3.4 50 14.1 49 36.9 10.3 - 10.4 34 36.6 33 30.4 3.4 - 3.5 49 18.6 48 33.4 10.4 - 10.5 31 46.9 29 24.1 3.5 - 3.6 48 25.2 47 27.8 10.5 - 10.6 29 46.5 28 25.5 3.6 - 3.7 48 27.5 47 25.5 10.6 - 10.7 28 34.7 30 35.3 3.7 - 3.8 48 28.9 47 24.1 10.7 - 10.8 28 30.8 27 42.2 3.8 - 3.9 50 23.2 49 27.8 10.8 - 1.09 27 33.8 28 38.2 3.9 - 4.0 45 27.5 44 28.5 10.9 - 11.0 25 30.8 25 44.2 4.0 - 4.1 42 34.7 41 24.3 11.0 - 11.1 28 39.9 28 32.1 4.1 - 4.2 48 25.5 47 27.5 11.1 - 11.2 30 37.3 29 33.7 4.2 - 4.3 51 19.6 50 30.4 11.2 - 11.3 29 36.5 28 35.5 4.3 - 4.4 53 19.3 52 28.7 11.3 - 11.4 28 33.7 27 39.3 4.4 - 4.5 54 11.7 53 35.3 11.4 - 11.5 28 36.1 29 34.9 4.5 - 4.6 53 10.8 52 37.2 11.5 - 11.6 28 40 27 33 4.6 - 4.7 54 14.7 53 32.3 11.6 - 11.7 30 40 27 33 4.7 - 4.8 53 10.9 52 37.1 11.7 - 11.8 33 22 32 46 4.8 - 4.9 52 19.2 51 29.8 11.8 - 11.9 29 40.1 25 34.9 4.9 - 5.0 55 15.4 54 30.6 11.9 - 12.0 25 39.4 25 35.6 5.0 - 5.1 54 14.3 53 32.7 12.0 - 12.1 26 46.3 24 29.7 5.1 - 5.2 59 2 58 40 12.1 - 12.2 28 35.7 27 37.3 5.2 - 5.3 60 4.8 59 36.2 12.2 - 12.3 28 48 26 26 5.3 - 5.4 60 9.8 59 31.2 12.3 - 12.4 28 40 27 33 5.4 - 5.5 59 17.8 58 24.2 12.4 - 12.5 28 46.8 25 28.2 5.5 - 5.6 57 14.9 56 29.1 12.5 - 12.6 28 30.6 27 42.4 5.6 - 5.7 57 15.4 56 28.6 12.6 - 12.7 28 32.5 27 40.5 5.7 - 5.8 54 11.2 53 35.8 12.7 - 12.8 28 31.4 27 41.6 5.8 - 5.9 55 12.9 54 33.1 12.8 - 12.9 26 44.4 23 32.6 5.9 - 6.0 53 13.2 52 34.8 12. 9 -13.0 24 42.2 24 33.8 6.0 - 6.1 58 0.7 57 42.3 13.0 - 13.1 25 40 27 33 6.1 - 6.2 60 3.1 59 37.9 13.1 - 13.2 26 30.7 26 43.3 6.2 - 6.3 64 7.7 63 29.3 13.2 - 13.3 29 30.5 27 42.5 6.3 - 6.4 62 7.9 61 31.1 13.3 - 13.4 31 32 30 38 6.4 - 6.5 59 7.3 58 34.7 13.4 - 13.5 31 32.7 27 40.3 6.5 - 6.6 64 0.8 63 36.2 13.5 - 13.6 32 38 31 31 6.6 - 6.7 61 6.3 60 33.7 13.6 - 13.7 32 31.9 29 39.1 6.7 - 6.8 63 7.1 62 30.9 13.7 - 13.8 33 38.8 32 29.2 6.8 - 6.9 62 6.9 61 32.1 13.8 - 13.9 32 30.4 28 41.6 6.9 - 7.0 60 4.5 59 36.5 13.9 - 14.0 31 32.2 30 37.8 14.0 - 14.1 30 37.4 27 35.6 14.1 - 14.2 30 39.4 29 31.6 14.2 - 14.3 30 39.5 29 31.5 14.3 - 14.4 30 34 29 37 14.4 - 14.5 30 37.8 31 31.2 14.5 - 14.6 30 20.8 29 50.2 14.6 - 14.7 31 38.4 29 32.6 14.7 - 14.8 32 37 31 32 14.8 - 14.9 31 38.9 31 30.1 14.9 - 15.0 31 37.2 30 32.8 Three phase distribution (%)water amount (mm) Three phase distribution (%)S1 core depth (m) S1 core depth (m) water amount (mm) Table A2. Soil water content (mm) and three phase distribution (%) of 0.1 m core samples. G eo lo gi a C ro at ic a Geologia Croatica 71/278 Gas phase Liquid phase Solid phase Gas phase Liquid phase Solid phase 0.0 - 0.1 32 35.8 31 33.2 5.0 - 5.1 65 11.6 64 24.4 0.1- 0.2 39 29 38 33 5.1 - 5.2 66 10.2 65 24.8 0.2 - 0.3 47 12.5 46 41.5 5.2 - 5.3 66 8.4 65 26.6 0.3 - 0.4 46 12 45 43 5.3 - 5.4 72 4.5 71 24.5 0.4 - 0.5 52 26.4 51 22.6 5.4 - 5.5 69 9.9 68 22.1 0.5 - 0.6 60 13.7 59 27.3 5.5 - 5.6 68 10.5 67 22.5 0.6 - 0.7 61 17.4 60 22.6 5.6 - 5.7 66 11.7 65 23.3 0.7 - 0.8 67 16.5 66 17.5 5.7 - 5.8 68 11.5 67 21.5 0.8 - 0.9 69 12.9 68 19.1 5.8 - 5.9 69 9.7 68 22.3 0.9 - 1.0 63 26 62 12 5.9 - 6.0 67 8.8 66 25.2 1.0 - 1.1 68 13.1 67 19.9 6.0 - 6.1 65 7.5 64 28.5 1.1 - 1.2 58 10.5 57 32.5 6.1 - 6.2 67 4.8 66 29.2 1.2 - 1.3 71 18.5 70 11.5 6.2 - 6.3 63 11.5 62 26.5 1.3 - 1.4 72 2.1 71 26.9 6.3 - 6.4 62 6.2 61 32.8 1.4 - 1.5 69 17.1 68 14.9 6.4 - 6.5 87 10.5 55 34.5 1.5 -1.6 71 18 70 12 6.5 - 6.6 62 4.4 61 34.6 1.6 - 1.7 68 16 67 17 6.6 - 6.7 61 3 60 37 1.7 - 1.8 64 28.6 63 8.4 6.7 - 6.8 60 4 59 37 1.8 - 1.9 67 12.9 66 21.1 6.8 - 6.9 57 4.8 56 39.2 1.9 - 2.0 75 5 74 21 6.9 - 7.0 57 7.2 56 36.8 2.0 - 2.1 77 6 76 18 7.0 - 7.1 61 0.2 60 39.8 2.1 - 2.2 77 5.4 76 18.6 7.1 - 7.2 53 1.2 52 46.8 2.2 - 2.3 76 4.8 75 20.2 7.2 - 7.3 56 6.2 55 38.8 2.3 - 2.4 76 5.5 75 19.5 7.3 - 7.4 55 3.8 54 42.2 2.4 - 2.5 76 6.6 75 18.4 7.4 - 7.5 55 6.1 54 39.9 2.5 - 2.6 68 17.7 67 15.3 7.5 - 7.6 53 7.2 52 40.8 2.6 - 2.7 72 2.3 71 26.7 7.6 - 7.7 53 14.8 52 33.2 2.7 - 2.8 71 10 70 20 7.7 - 7.8 51 6.4 50 43.6 2.8 - 2.9 74 11 73 16 7.8 - 7.9 52 3.4 51 45.6 2.9 - 3.0 70 14.7 69 16.3 7.9 - 8.0 53 1.2 52 46.8 3.0 - 3.1 67 5 66 29 8.0 - 8.1 55 0.6 54 45.4 3.1 - 3.2 66 2.6 65 32.4 8.1 - 8.2 54 1.9 53 45.1 3.2 - 3.3 69 18.4 68 13.6 8.2 - 8.3 51 4.8 50 45.2 3.3 - 3.4 67 13.4 66 20.6 8.3 - 8.4 53 2.8 52 45.2 3.4 - 3.5 69 6.9 68 25.1 8.4 - 8.5 53 4 52 44 3.5 - 3.6 68 17.8 67 15.2 8.5 - 8.6 52 3.6 51 45.4 3.6 - 3.7 60 7.9 59 33.1 8.6 - 8.7 48 5.5 47 47.5 3.7 - 3.8 67 2.8 66 31.2 8.7 - 8.8 52 3.7 51 45.3 3.8 - 3.9 69 6.1 68 25.9 8.8 - 8.9 51 3.1 50 46.9 3.9 - 4.0 59 17.4 58 24.6 8.9 - 9.0 50 3 49 48 4.0 - 4.1 67 5 66 29 9.0 - 9.1 53 0.3 52 47.7 4.1 - 4.2 68 2.8 67 30.2 9.1 - 9.2 52 1.1 51 47.9 4.2 - 4.3 65 2.2 64 33.8 9.2 - 9.3 52 2.3 51 46.7 4.3 - 4.4 55 8.2 54 37.8 9.3 - 9.4 52 2.4 51 46.6 4.4 - 4.5 69 3.8 68 28.2 9.4 - 9.5 50 5.7 49 45.3 4.5 - 4.6 59 4.9 58 37.1 9.5 - 9.6 151 7 48 45 4.6 - 4.7 49 6 48 46 9.6 - 9.7 48 7.4 47 45.6 4.7 - 4.8 48 14.3 47 38.7 9.7 - 9.8 49 5.9 48 46.1 4.8 - 4.9 47 22.6 46 31.4 9.8 - 9.9 53 1.3 52 46.7 4.9 - 5.0 49 24.4 48 27.6 9.9 - 10.0 52 4.6 51 44.4 10.0 - 10.1 53 2.4 52 45.6 Three phase distribution (%)C3 core depth (m) water amount (mm) Three phase distribution (%) C3 core depth (m) water amount (mm) Table A2. Continuation. G eologia C roatica Okumura et al.: Evaluations of the downward velocity of soil water movement in the unsaturated zone in a groundwater recharge area ... 79 Gas phase Liquid phase Solid phase Gas phase Liquid phase Solid phase 0.0 - 0.2 144 25 47 28 0.0 - 0.2 77 23 38 39 0.2 - 0.4 98 25.4 48 26.6 0.2 - 0.4 116 28.9 57 14.1 0.4 - 0.6 96 30.6 47 22.4 0.4 - 0.6 120 12.5 59 28.5 0.6 - 0.8 94 24.8 46 29.2 0.6 - 0.8 108 30 53 17 0.8 - 1.0 92 26 55 19 0.8 - 1.0 118 27.3 58 14.7 1.0 - 1.2 100 n.d. n.d. n.d. 1.0 - 1.2 119 n.d. n.d. n.d. 1.2 - 1.4 98 n.d. n.d. n.d. 1.2 - 1.4 126 n.d. n.d. n.d. 1.4 - 1.6 100 n.d. n.d. n.d. 1.4 - 1.6 130 11 64 25 1.6 - 1.8 112 n.d. n.d. n.d. 1.6 - 1.8 130 17.5 64 18.5 1.8 - 2.0 108 n.d. n.d. n.d. 1.8 - 2.0 132 16.5 65 18.5 2.0 - 2.2 100 n.d. n.d. n.d. 2.0 - 2.2 141 n.d. 69 n.d. 2.2 - 2.4 90 n.d. n.d. n.d. 2.2 - 2.4 149 4.7 73 22.3 2.4 - 2.6 77 n.d. n.d. n.d. 2.4 - 2.6 145 4.4 71 24.6 2.6 - 2.8 73 n.d. n.d. n.d. 2.6 - 2.8 143 2.2 70 27.8 2.8 - 3.0 79 n.d. n.d. n.d. 2.8 - 3.0 143 3.5 70 26.5 3.0 - 3.2 82 n.d. n.d. n.d. 3.0 - 3.2 139 11.4 68 20.6 3.2 - 3.4 84 n.d. n.d. n.d. 3.2 - 3.4 132 16.7 65 18.3 3.4 - 3.6 73 n.d. n.d. n.d. 3.4 - 3.6 139 9 68 23 3.6 - 3.8 82 n.d. n.d. n.d. 3.6 - 3.8 141 19.5 69 11.5 3.8 - 4.0 73 n.d. n.d. n.d. 3.8 - 4.0 135 18.5 66 15.5 4.0 - 4.2 96 n.d. n.d. n.d. 4.0 - 4.2 130 3.5 64 32.5 4.2 -4.4 63 n.d. n.d. n.d. 4.2 -4.4 124 17.5 61 21.5 4.4 - 4.6 128 n.d. n.d. n.d. 4.4 - 4.6 102 21.4 50 28.6 4.6 - 4.8 100 n.d. n.d. n.d. 4.6 - 4.8 120 11.8 59 29.2 4.8 - 5.0 104 16.5 55 28.5 4.8 - 5.0 115 n.d. 56.5 n.d. 5.0 - 5.2 110 17.8 52.5 29.7 5.0 - 5.2 110 16.9 54 29.1 5.2 - 5.4 102 n.d. n.d. n.d. 5.2 - 5.4 102 12 50 38 5.4 - 5.6 106 n.d. n.d. n.d. 5.4 - 5.6 102 11.5 50 38.5 5.6 - 5.8 112 n.d. n.d. n.d. 5.6 - 5.8 108 9.7 53 37.3 5.8 - 6.0 96 n.d. n.d. n.d. 5.8 - 6.0 105 n.d. 51.5 n.d. 6.0 - 6.2 104 n.d. n.d. n.d. 6.0 - 6.2 102 19.3 50 30.7 6.2 - 6.4 106 n.d. n.d. n.d. 6.2 - 6.4 108 2.9 53 44.1 6.4 - 6.6 108 n.d. n.d. n.d. 6.4 - 6.6 110 19 54 27 6.6 - 6.8 110 n.d. n.d. n.d. 6.6 - 6.8 104 13 51 36 6.8 - 7.0 106 n.d. n.d. n.d. 6.8 - 7.0 105 n.d. 51.5 n.d. 7.0 - 7.2 102 n.d. n.d. n.d. 7.0 - 7.2 106 12 52 36 7.2 - 7.4 110 n.d. n.d. n.d. 7.2 - 7.4 102 28 50 22 7.4 - 7.6 135 n.d. n.d. n.d. 7.4 - 7.6 104 28.7 51 20.3 7.6 - 7.8 118 n.d. n.d. n.d. 7.6 - 7.8 92 22.9 45 32.1 7.8 - 8.0 110 n.d. n.d. n.d. 7.8 - 8.0 94 n.d. 46 n.d. 8.0 - 8.2 122 n.d. n.d. n.d. 8.0 - 8.2 96 24 47 29 8.2 - 8.4 112 n.d. n.d. n.d. 8.2 - 8.4 92 23 45 32 8.4 - 8.6 108 n.d. n.d. n.d. 8.4 - 8.6 98 26.6 48 25.4 8.6 - 8.8 112 n.d. n.d. n.d. 8.6 - 8.8 100 29.1 49 21.9 8.8 - 9.0 108 n.d. n.d. n.d. 8.8 - 9.0 100 12.4 49 38.6 9.0 - 9.2 106 n.d. n.d. n.d. 9.0 - 9.2 104 18.3 51 30.7 9.2 - 9.4 90 n.d. n.d. n.d. 9.2 - 9.4 104 16 51 33 9.4 - 9.6 104 n.d. n.d. n.d. 9.4 - 9.6 104 16.5 51 32.5 9.6 - 9.8 100 n.d. n.d. n.d. 9.6 - 9.8 100 13.7 49 37.3 9.8 - 10.0 52 18.3 47 34.7 9.8 - 10.0 104 16.6 51 32.4 10.0 - 10.2 102 15.6 50 34.4 10.2 - 10.4 102 16.6 50 33.4 10.4 - 10.6 102 16.3 50 33.7 10.6 - 10.8 104 15.5 51 33.5 10.8 - 11.0 106 1.5 52 46.5 11.0 - 11.2 100 19.3 49 31.7 11.2 - 11.4 96 17 47 36 11.4 - 11.6 98 16.4 48 35.6 11.6 - 11.8 90 11 44 45 11.8 - 12.0 78 n.d. 38.5 n.d. 12.0 - 12.2 67 37.2 33 29.8 12.2 - 12.4 55 30.7 27 42.3 12.4 - 12.6 55 31.6 27 41.4 12.6 - 12.8 49 30.1 24 45.9 12.8 - 13.0 49 n.d. n.d. n.d. 13.0 - 13.2 49 31.5 24 44.5 13.2 - 13.4 45 30.1 22 47.9 13.4 - 13.6 47 30.5 23 46.5 13.6 - 13.8 49 31 24 45 13.8 - 14.0 46 n.d. n.d. n.d. 14.0 - 14.2 47 n.d. n.d. n.d. 14.2 - 14.4 43 40 21 39 14.4 - 14.6 49 34.2 24 41.8 14.6 - 14.8 46 n.d. n.d. n.d. 14.8 - 15.0 48 n.d. n.d. n.d. Three phase distribution (%)C1 core depth (m) water amount (mm) Three phase distribution (%) C2 core depth (m) water amount (mm) Table A2. Continuation. G eo lo gi a C ro at ic a Geologia Croatica 71/280 Table A2. Continuation. Gas phase Liquid phase Solid phase Gas phase Liquid phase Solid phase 0.0 - 0.1 51 13.9 50 36.1 7.0 - 7.1 45 6.7 44 49.3 0.1- 0.2 47 9.4 46 44.6 7.1 - 7.2 44 2.5 43 54.5 0.2 - 0.3 47 27.9 46 26.1 7.2 - 7.3 41 9.9 40 50.1 0.3 - 0.4 50 19.8 49 31.2 7.3 - 7.4 42 18.2 41 40.8 0.4 - 0.5 50 22.6 49 28.4 7.4 - 7.5 46 6.3 45 48.7 0.5 - 0.6 50 36.9 49 14.1 7.5 - 7.6 47 10 46 44 0.6 - 0.7 47 21.3 46 32.7 7.6 - 7.7 42 18.2 41 40.8 0.7 - 0.8 53 25.2 52 22.8 7.7 - 7.8 43 1.3 42 56.7 0.8 - 0.9 53 28.9 52 19.1 7.8 - 7.9 41 11.9 40 48.1 0.9 - 1.0 54 29.2 53 17.8 7.9 - 8.0 41 15.9 40 44.1 1.0 - 1.1 50 34.4 49 16.6 8.0 - 8.1 44 18.6 43 38.4 1.1 - 1.2 58 14 57 29 8.1 - 8.2 49 4.7 48 47.3 1.2 - 1.3 45 35.5 44 20.5 8.2 - 8.3 37 9.9 36 54.1 1.3 - 1.4 54 8.8 53 38.2 8.3 - 8.4 46 16 45 39 1.4 - 1.5 58 17.7 57 25.3 8.4 - 8.5 37 21.7 36 42.3 1.5 -1.6 54 10.9 53 36.1 8.5 - 8.6 38 11.3 37 51.7 1.6 - 1.7 63 10.7 62 27.3 8.6 - 8.7 36 38.7 35 26.3 1.7 - 1.8 61 9.8 60 30.2 8.7 - 8.8 36 20.8 35 44.2 1.8 - 1.9 54 19.8 53 27.2 8.8 - 8.9 35 38.8 34 27.2 1.9 - 2.0 55 10.5 54 35.5 8.9 - 9.0 35 21.9 34 44.1 2.0 - 2.1 59 17.2 58 24.8 9.0 - 9.1 34 38.8 33 28.2 2.1 - 2.2 59 16 58 26 9.1 - 9.2 36 38 35 27 2.2 - 2.3 66 17.5 65 17.5 9.2 - 9.3 39 23.6 38 38.4 2.3 - 2.4 66 8.9 65 26.1 9.3 - 9.4 38 22.9 37 40.1 2.4 - 2.5 64 18 63 19 9.4 - 9.5 37 39 36 25 2.5 - 2.6 57 18.7 56 25.3 9.5 - 9.6 36 39 35 26 2.6 - 2.7 59 1.2 58 40.8 9.6 - 9.7 38 24.1 37 38.9 2.7 - 2.8 62 5 61 34 9.7 - 9.8 38 24.5 37 38.5 2.8 - 2.9 55 5.4 54 40.6 9.8 - 9.9 37 22.9 36 41.1 2.9 - 3.0 57 1.3 56 42.7 9.9 - 10.0 35 24.6 34 41.4 3.0 - 3.1 54 8.5 53 38.5 10.0 - 10.1 45 14.9 44 41.1 3.1 - 3.2 54 8.7 53 38.3 10.1 - 10.2 40 18.4 39 42.6 3.2 - 3.3 53 9.4 52 38.6 10.2 - 10.3 47 15 46 39 3.3 - 3.4 51 9 50 41 10.3 - 10.4 45 12.6 44 43.4 3.4 - 3.5 47 2.8 46 51.2 10.4 - 10.5 47 16.5 46 37.5 3.5 - 3.6 54 4.5 53 42.5 10.5 - 10.6 39 5.4 38 56.6 3.6 - 3.7 52 16 51 33 10.6 - 10.7 50 3 49 48 3.7 - 3.8 53 8.8 52 39.2 10.7 - 10.8 50 1.8 49 49.2 3.8 - 3.9 55 3 54 43 10.8 - 1.09 45 13.3 44 42.7 3.9 - 4.0 59 8.2 58 33.8 10.9 - 11.0 49 18.1 48 33.9 4.0 - 4.1 52 4.3 51 44.7 11.0 - 11.1 49 18.1 48 33.9 4.1 - 4.2 58 4.5 57 38.5 11.1 - 11.2 50 10.2 49 40.8 4.2 - 4.3 55 15 54 31 11.2 - 11.3 50 2.6 49 48.4 4.3 - 4.4 54 1.8 53 45.2 11.3 - 11.4 49 1.3 48 50.7 4.4 - 4.5 56 1.6 55 43.4 11.4 - 11.5 50 5.1 49 45.9 4.5 - 4.6 57 4.6 56 39.4 11.5 - 11.6 52 3.8 51 45.2 4.6 - 4.7 53 1.2 52 46.8 11.6 - 11.7 51 9.3 50 40.7 4.7 - 4.8 48 19.5 47 33.5 11.7 - 11.8 45 16.2 44 39.8 4.8 - 4.9 51 18.3 50 31.7 11.8 - 11.9 47 6 46 48 4.9 - 5.0 54 16.8 53 30.2 11.9 - 12.0 51 4.3 50 45.7 5.0 - 5.1 58 1.1 57 41.9 12.0 - 12.1 53 2 52 46 5.1 - 5.2 62 5.9 61 33.1 12.1 - 12.2 57 3.3 56 40.7 5.2 - 5.3 60 3.8 59 37.2 12.2 - 12.3 53 17 52 31 5.3 - 5.4 60 2.1 59 38.9 12.3 - 12.4 56 2 55 43 5.4 - 5.5 59 2.4 58 39.6 12.4 - 12.5 59 6.4 58 35.6 5.5 - 5.6 47 26.1 46 27.9 12.5 - 12.6 55 3.6 54 42.4 5.6 - 5.7 53 18.9 52 29.1 12.6 - 12.7 52 10 51 39 5.7 - 5.8 57 4.5 56 39.5 12.7 - 12.8 54 4 53 43 5.8 - 5.9 56 1.2 55 43.8 12.8 - 12.9 56 4.9 55 40.1 5.9 - 6.0 56 4.7 55 40.3 12. 9 -13.0 51 16 50 34 6.0 - 6.1 53 7 52 41 13.0 - 13.1 60 6.2 59 34.8 6.1 - 6.2 52 8.2 51 40.8 13.1 - 13.2 57 7 56 37 6.2 - 6.3 50 5.6 49 45.4 13.2 - 13.3 54 8.3 53 38.7 6.3 - 6.4 51 7 50 43 13.3 - 13.4 60 4.5 59 36.5 6.4 - 6.5 46 8.6 45 46.4 13.4 - 13.5 62 6.4 61 32.6 6.5 - 6.6 55 9.2 54 36.8 13.5 - 13.6 54 8.2 53 38.8 6.6 - 6.7 50 8.6 49 42.4 13.6 - 13.7 58 5.9 57 37.1 6.7 - 6.8 53 8.9 52 39.1 13.7 - 13.8 57 5.3 56 38.7 6.8 - 6.9 48 7 47 46 13.8 - 13.9 56 10 55 35 6.9 - 7.0 51 1.9 50 48.1 13.9 - 14.0 56 10.4 55 34.6 Three phase distribution (%)S2 core depth (m) water amount (mm) Three phase distribution (%) S2 core depth (m) water amount (mm) G eologia C roatica Okumura et al.: Evaluations of the downward velocity of soil water movement in the unsaturated zone in a groundwater recharge area ... 81 Table A3. Precipitation data using DFM calculation for all cores. total amount(mm) δD (‰) δ18O (‰) d-excess (‰) total amount(mm) δD (‰) δ18O (‰) d-excess (‰) Jan-2005 5 48 -50 -9.5 26 Jan-2011 3 3 -40 -8.6 28.2 Feb-2005 6 100 -44 -7.6 16.8 Feb-2011 8 40 -58 -10.0 21.9 Mar-2005 9 128 -24 -5.1 16.8 Mar-2011 8 51 -30 -6.7 23.7 Apr-2005 17 92 -14 -3.2 11.6 Apr-2011 15 67 -14 -4.1 18.6 May-2005 21 135 -26 -4.6 10.8 May-2011 20 126 -79 -10.3 4.2 Jun-2005 26 93 -38 -5.9 9.2 Jun-2011 24 929 -69 -10.0 10.8 Jul-2005 28 365 -48 -7.4 11.2 Jul-2011 28 253 -50 -7.4 9.4 Aug-2005 28 73 -66 -9.7 11.6 Aug-2011 28 385 -44 -6.6 9.0 Sep-2005 27 147 -89 -11.7 4.6 Sep-2011 25 76 -74 -9.8 4.8 Oct-2005 21 41 -20 -4.4 15.2 Oct-2011 19 107 -40 -6.8 14.0 Nov-2005 14 73 -18 -4.9 21.2 Nov-2011 16 89 -38 -6.9 16.6 Dec-2005 5 31 -16 -6.3 34.4 Dec-2011 7 33 n.d. n.d. n.d. Jan-2006 6 61 -40 -6.6 12.8 Jan-2012 5 15 -64 -10.1 16.6 Feb-2006 8 118 -28 -5.8 18.4 Feb-2012 6 32 -33 -6.3 17.5 Mar-2006 10 102 -20 -4.9 19.2 Mar-2012 11 90 -21 -4.2 12.0 Apr-2006 15 216 -14 -3.3 12.4 Apr-2012 16 42 -38 -5.8 9.1 May-2006 21 214 -21 -4.3 13.4 May-2012 21 25 -61 -7.9 2.1 Jun-2006 24 642 -51 -7.8 11.4 Jun-2012 23 223 -53 -7.4 6.8 Jul-2006 28 789 -39 -6.1 9.8 Jul-2012 28 183 -41 -6.5 11.0 Aug-2006 29 428 -62 -8.6 6.8 Aug-2012 29 35 -55 -8.1 9.7 Sep-2006 25 94 -33 -5.9 14.2 Sep-2012 25 24 -74 -10.0 5.9 Oct-2006 21 11 -7 -2.6 13.8 Oct-2012 19 39 -22 -5.1 18.0 Nov-2006 15 81 -56 -8.9 15.2 Nov-2012 12 21 -35 -7.0 21.3 Dec-2006 9 48 -42 -7.4 17.2 Dec-2012 6 14 -16 -4.9 24.0 Jan-2007 7 34 0 -3.3 26.4 Jan-2013 5 45 -96 -13.3 10.9 Feb-2007 10 76 -16 -4.7 21.6 Feb-2013 7 167 -23 -5.5 20.7 Mar-2007 12 105 -20 -4.7 17.6 Mar-2013 12 110 -17 -4.0 15.8 Apr-2007 15 109 -38 -6.4 13.2 Apr-2013 15 164 -19 -4.4 15.8 May-2007 21 141 -31 -5.2 10.6 May-2013 21 54 -30 -4.8 8.2 Jun-2007 24 184 -63 -8.7 6.6 Jun-2013 24 308 -57 -8.5 10.6 Jul-2007 27 675 -67 -9 5 Jul-2013 29 119 -38 -6.2 11.8 Aug-2007 29 176 -43 -5.7 2.6 Aug-2013 29 571 -52 -7.8 11.0 Sep-2007 27 81 -30 -4.9 9.2 Sep-2013 25 199 -89 -12.7 12.7 Oct-2007 21 135 n.d. n.d. n.d. Oct-2013 21 109 -43 -6.6 9.1 Nov-2007 13 31 -27 -6.9 28.2 Nov-2013 12 80 -35 -6.7 18.8 Dec-2007 9 67 -25 -5.6 19.8 Dec-2013 7 51 -68 -10.1 13.1 Jan-2008 7 137 n.d. n.d. n.d. Jan-2014 6 36 -18 -5.4 25.5 Feb-2008 5 44 n.d. n.d. n.d. Feb-2014 7 121 -41 -7.5 19.0 Mar-2008 11 91 n.d. n.d. n.d. Mar-2014 11 130 -35 -6.1 13.2 Apr-2008 16 116 -42 -6.7 11.8 Apr-2014 16 69 -14 -3.5 14.5 May-2008 20 210 -54 -7.1 2.8 May-2014 20 135 -50 -7.4 9.1 Jun-2008 23 776 -66 -9.1 6.7 Jun-2014 23 259 -84 -11.3 6.6 Jul-2008 29 204 -67 -9.2 7.2 Jul-2014 27 358 -31 -4.4 4.6 Aug-2008 28 227 -53 -7.9 10.7 Aug-2014 27 213 -48 -7.4 11.0 Sep-2008 26 295 -79 -11.2 10.4 Sep-2014 24 107 -52 -7.9 11.5 Oct-2008 20 62 -9 -5.1 32.4 Oct-2014 20 142 -29 -5.3 13.8 Nov-2008 13 89 -11 -8.2 54.9 Nov-2014 14 63 -40 -7.1 16.7 Dec-2008 8 106 -11 -3.6 17.8 Dec-2014 6 63 -23 -6.6 29.4 Jan-2009 6 55 -21 -5.4 21.8 Jan-2015 7 100 -31 -6.1 17.6 Feb-2009 10 134 -15 -4.3 18.8 Feb-2015 7 34 -21 -5.3 21.0 Mar-2009 11 145 -32 -5.4 11.9 Mar-2015 11 186 -23 -5.7 22.2 Apr-2009 16 80 -42 -6.8 13.2 Apr-2015 17 151 -11 -2.9 11.8 May-2009 21 69 -37 -5.3 5.6 May-2015 21 131 -36 -5.7 9.7 Jun-2009 24 246 -45 -6.7 8.9 Jun-2015 22 628 -39 -6.4 11.8 Jul-2009 27 429 -53 -7.8 10.1 Jul-2015 26 376 -53 -8.0 10.8 Aug-2009 29 67 -53 -7.1 4.2 Aug-2015 27 246 -61 -8.6 8.1 Sep-2009 26 34 -27 -4.7 10.6 Sep-2015 24 150 -64 -9.2 9.5 Oct-2009 19 130 -35 -5.0 5.2 Oct-2015 19 65 -70 -10.0 10.2 Nov-2009 13 112 -69 -10.2 12.1 Nov-2015 16 137 2 -2.7 22.9 Dec-2009 8 67 -44 -7.9 19.4 Dec-2015 10 92 -49 -8.2 16.2 Jan-2010 6 48 -25 -5.3 17.2 Jan-2016 6 71 -20 -5.0 19.7 Feb-2010 10 192 -25 -4.6 12.0 Feb-2016 7 74 -64 -10.3 18.3 Mar-2010 11 177 -25 -6.7 29.1 Mar-2016 11 60 -35 -7.2 22.8 Apr-2010 15 226 -27 -4.5 8.5 Apr-2016 17 179 -47 -8.3 19.7 May-2010 20 285 -29 -4.6 8.2 May-2016 21 273 -37 -7.1 20.6 Jun-2010 24 401 -85 -11.6 7.9 Jun-2016 24 644 -5 -2.5 15.1 Jul-2010 27 362 -42 -6.0 5.9 Jul-2016 28 390 -19 -3.8 11.6 Aug-2010 30 58 -43 -5.5 1.3 Sep-2010 26 118 -43 -6.5 9.2 Oct-2010 20 85 -40 -6.7 13.3 Nov-2010 12 29 -34 -7.2 22.9 Dec-2010 8 94 -40 -7.7 21.1 month month average temperature (℃) precipitationprecipitationaverage temperature (℃) G eo lo gi a C ro at ic a Geologia Croatica 71/282