Impact of climate forcing uncertainty and human water use on global and continental water balance components

Abstract

The assessment of water balance components using global hydrological models is subject to climate forcing uncertainty as well as to an increasing intensity of human water use within the 20th century. The uncertainty of five state-of-the-art climate forcings and the resulting range of cell runoff that is simulated by the global hydrological model WaterGAP is presented. On the global land surface, about 62% of precipitation evapotranspires, whereas 38% discharges into oceans and inland sinks. During 1971-2000, evapotranspiration due to human water use amounted to almost 1% of precipitation, while this anthropogenic water flow increased by a factor of approximately 5 between 1901 and 2010. Deviation of estimated global discharge from the ensemble mean due to climate forcing uncertainty is approximately 4%. Precipitation uncertainty is the most important reason for the uncertainty of discharge and evapotranspiration, followed by shortwave downward radiation. At continental levels, deviations of water balance components due to uncertain climate forcing are higher, with the highest discharge deviations occurring for river discharge in Africa (-6 to 11% from the ensemble mean). Uncertain climate forcings also affect the estimation of irrigation water use and thus the estimated human impact of river discharge. The uncertainty range of global irrigation water consumption amounts to approximately 50% of the global sum of water consumption in the other water use sector.

WaterResourcesAssessmentandSeasonalPrediction

Proc. IAHS, 374, 5362, 2016 proc-iahs.net/374/53/2016/ doi:10.5194/piahs-374-53-2016 Author(s) 2016. CC Attribution 3.0 License.

Hannes Mller Schmied1,2, Linda Adam1, Stephanie Eisner3, Gabriel Fink3, Martina Flrke3, Hyungjun Kim4, Taikan Oki4, Felix Theodor Portmann1, Robert Reinecke1, Claudia Riedel1, Qi Song1, Jing Zhang1, and Petra Dll1

1Institute of Physical Geography, Goethe University Frankfurt, Frankfurt, Germany

2Senckenberg Biodiversity and Climate Research Centre (BiK-F), Frankfurt, Germany

3Center for Environmental Systems Research (CESR), University of Kassel, Kassel, Germany

4Institute of Industrial Science, The University of Tokyo, Tokyo, Japan

Correspondence to: Hannes Mller Schmied ([email protected])

Published: 17 October 2016

Abstract. The assessment of water balance components using global hydrological models is subject to climate forcing uncertainty as well as to an increasing intensity of human water use within the 20th century. The uncertainty of ve state-of-the-art climate forcings and the resulting range of cell runoff that is simulated by the global hydrological model WaterGAP is presented. On the global land surface, about 62 % of precipitation evapotranspires, whereas 38 % discharges into oceans and inland sinks. During 19712000, evapotranspiration due to human water use amounted to almost 1 % of precipitation, while this anthropogenic water ow increased by a factor of approximately 5 between 1901 and 2010. Deviation of estimated global discharge from the ensemble mean due to climate forcing uncertainty is approximately 4 %. Precipitation uncertainty is the most important reason for the uncertainty of discharge and evapotranspiration, followed by shortwave downward radiation. At continental levels, deviations of water balance components due to uncertain climate forcing are higher, with the highest discharge deviations occurring for river discharge in Africa (6 to 11 % from the ensemble mean). Un

certain climate forcings also affect the estimation of irrigation water use and thus the estimated human impact of river discharge. The uncertainty range of global irrigation water consumption amounts to approximately 50 % of the global sum of water consumption in the other water use sector.

1 Introduction

The interest in global-scale water resources assessments has increased in the last two decades. There has been an increasing number of publications in this eld (Web of Science, topic global scale AND water resources, 19811990: 0 entries; 19912000: 6 entries; 20012010: 64 entries; 20112015: 85 entries), and a number of global hydrological models (GHMs) have been developed (Bierkens, 2015).The UN and other international organizations require global-scale information on water resources and their use, e.g. UNESCOs World Water Assessment Programme (http://www.unesco.org/water/wwap

Web End =www.unesco. http://www.unesco.org/water/wwap

Web End =org/water/wwap ) or the Transboundary Waters AssessmentProgramme (TWAP, http://www.geftwap.org/twap-project

Web End =http://www.geftwap.org/twap-project http://www.geftwap.org/twap-project

Web End = ),

Impact of climate forcing uncertainty and human water use on global and continental water balance components

which can only be provided by modelling approaches due to a lack of observations with global coverage. Such model-based assessments require meteorological variables as climate forcing input. Currently, a number of state-of-the-art global-scale climate forcings are available that are all based on weather models and differ in terms of methodology including the underlying reanalysis and in terms of observation data used for bias correction. Different climate forcings result in large differences in simulated water uxes and states as has already been shown by Biemans et al. (2009) for precipitation uncertainty and by Mller Schmied et al. (2014) regarding the uncertainty caused by two climate forcings that differ with respect to other climate variables. Analyses of the impact of different climate forcings are currently the focus of

Published by Copernicus Publications on behalf of the International Association of Hydrological Sciences.

54 H. Mller Schmied et al.: Impact of climate forcing uncertainty and human water use

Table 1. Summary of climate forcing characteristics used in this study. Abbreviations: precipitation P , temperature T , shortwave downward radiation SWD, longwave downward radiation LWD.

Name Time span Basis Bias correction Reference

GSWP3 19012010 20th Century Reanalysis using NCEP atmosphere land model

GPCC v6 (P ), and undercatch correction (Hirabayashi et al., 2008) CRU TS3.21 (other variables)

http://hydro.iis.u-tokyo.ac.jp/GSWP3

Web End =http://hydro.iis.u-tokyo. http://hydro.iis.u-tokyo.ac.jp/GSWP3

Web End =ac.jp/GSWP3

PGFv2 19012012 NCEP-NCAR reanalysis CRU TS3.21 (P , T ), no precipitation undercatch correction, U Maryland, CRU TS3.21 cloud cover (SWD), U Maryland (LWD)

Updated version of Shefeld et al. (2006), information based on personal communication with J. Shefeld (2015)

WFD 19012001 ERA-40 reanalysis GPCCv4 (P ), undercatch correction using Adam and Lettenmaier (2003), CRU TS 2.1 cloud cover (SWD), CRU TS 2.1 temperature (T )

Weedon et al. (2010)

Weedon et al. (2014)

WFD_WFDEI 19012010 WFD 19011978,WFDEI (based on ERA-Interim reanalysis) afterwards

GPCC v5 (v6 for 2010) (P ), under-catch correction using Adam and Lettenmaier (2003), CRU TS 3.1/3.21 cloud cover (SWD), CRU TS 3.1/3.21 temperature (T )

WFDEI_hom 19012010 As WFD_WFDEI, but

WFD homogenized using a multiplicative approach for SWD and LWD and additive approach for T

Homogenization: Haddeland et al. (2012), Mller Schmied et al. (2016)

model intercomparison studies such as the Inter-Sectoral Impact Model Intercomparison Project (ISIMIP) in its phase 2a, where (among other sectors) several global and regional water models are driven by four state-of-the-art climate forcings and compared to historical observations of, for example, discharge and actual evapotranspiration. In particular, the propagation of climate forcing uncertainty at multiple scales (grid-cell level, continental, global) is one topic to be addressed in ISIMIP2a.

Humans increasingly inuence the water cycle through water abstractions (Oki and Kanae 2006), in particular for irrigation (e.g. Siebert et al., 2015) but also for other purposes like thermal power plant cooling, manufacturing, livestock production and domestic sectors (Flrke et al., 2013). Quantication of sectoral water abstractions and consumptive water use (also called water consumption, the amount of the abstracted water that evapotranspires during human water use or is incorporated in products), and in particular of the source of water, is highly uncertain due to lack of data (Dll et al., 2016). In some regions, irrigation by groundwater leads to groundwater depletion problems (Dll et al., 2014a; Wada, 2016), and it has been estimated that in groundwater depletion areas, farmers irrigate with only 70 % of the optimal amount of water (Dll et al., 2014a).

Given the large uncertainties, we aim to answer the following research questions by using the Water Global Assessment and Prognosis (WaterGAP) GHM in its version 2.2 (ISIMIP2a):

1. How does climate forcing affect computed runoff at the grid-cell level?

2. How does climate forcing uncertainty and human water use affect long-term average water balance components (including human water use) on global and continental scales?

In Sect. 2 we briey present the model and climate forcings used in this study. Results are presented and discussed in Sect. 3. The paper ends with a conclusion (Sect. 4), where we answer the research questions, followed by an outlook.

2 Data and methods

The global water availability and water use model WaterGAP (Alcamo et al., 2003; Dll et al., 2003; Mller Schmied et al., 2014) was applied using version WaterGAP 2.2 (ISIMIP2a).The main model characteristics of version 2.2 are described in Mller Schmied et al. (2014), and the differences to the ISIMIP2a version are described in Mller Schmied et

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H. Mller Schmied et al.: Impact of climate forcing uncertainty and human water use 55

al. (2016). WaterGAP has a spatial resolution of 0.5 0.5

(i.e. 55 55 km at the Equator) and consists of ve water

use models that are linked through the Ground Water Surface Water Use submodule with the WaterGAP global hydrology model (WGHM). Within WGHM, water storage changes in several compartments and freshwater uxes are modelled at a daily time step. WGHM is calibrated to match long-term average discharge at 1319 observation points (from GRDC database) within 1 % deviation by adjusting one to three parameters (calibration details in Mller Schmied et al., 2014).

Four state-of-the-art climate forcings provided by the Inter-Sectoral Impact Model Intercomparison Project (ISIMIP) in its current phase 2a (https://www.isimip.org/about/#simulation-rounds-isimip2a

Web End =https: https://www.isimip.org/about/#simulation-rounds-isimip2a

Web End =//www.isimip.org/about/#simulation-rounds-isimip2a https://www.isimip.org/about/#simulation-rounds-isimip2a

Web End = ) plus a fth homogenized forcing were used to force WaterGAP.Table 1 summarizes the main characteristics of all ve climate forcing datasets. For a detailed description, the reader is referred to Mller Schmied et al. (2016). The names of the model runs are similar to the names of the climate forcings.

3 Results and discussion

3.1 Global runoff at grid-cell level

Net cell runoff (computed as outow minus inow of each grid cell) differs considerably between the different climate forcing datasets (Fig. 1). This can be attributed to large differences between climate forcings at grid-cell level, in particular with respect to precipitation. Different observational datasets are used to bias-correct P (PGFv2 based on CRU and the others based on different versions of GPCC). This results in large differences (in both directions) at the regional scale for South America and South East Asia. Obviously, the unequal P gauging networks underlying the observational datasets and/or varying regionalization approaches lead to the large differences. In addition, PGFv2 is not corrected for under-catch of solid precipitation (J. Shefeld, personal communication, 2015) while all other datasets are. As undercatch correction (e.g. Adam and Lettenmaier, 2003) leads to the highest P increases in northern (snow-dominated) latitudes, P (and consequently net cell runoff) is lower for PGFv2 (red areas in the northern latitudes in Fig. 1b).

The main reason for the large discrepancies between GSWP3 and WFD in equatorial regions (Fig. 1c) is attributable to systematically smaller SWD (Fig. A3c) in energy-limited areas for the WFD dataset. This effect is lessened in the combined WFD_WFDEI dataset (Fig. 1d) and even more in the homogenized forcing WFDEI_hom (Fig. 1e), as WFDEI shows systematically higher SWD than WFD. The higher SWD in parts of Asia, western Africa and Australia (Fig. A3d, e) does not inuence net cell runoff signicantly because these regions are water-limited: evaporation and runoff are mainly controlled by precipitation and not by available energy. In many regions where SWD is in-

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Figure 1. Long-term (19712000) average net cell runoff of the model variants, displayed as absolute numbers for GSWP3 (a)

and differences to the other forcings, computed as PGFv2 minus GSWP3 (b), WFD minus GSWP3 (c), WFD_WFDEI minus

GSWP3 (d) and WFDEI_hom minus GSWP3 (e). Negative values in (a) indicate that water inow into cell from upstream and by precipitation is larger than outow due to evaporation from surface water bodies. All units in mm yr1.

56 H. Mller Schmied et al.: Impact of climate forcing uncertainty and human water use

Figure 2. Continental water balance components 19712000 (km3 yr1); ensemble mean of the ve climate forcings. Abbreviations: actual evapotranspiration (AET), discharge into oceans and inland sinks (Q), actual water consumption (WCa).

Table 2. Global water balance components for land area (except Antarctica and Greenland) in % of precipitation (row 1) for the ve model variants and 19712000. Cells representing inland sinks were excluded but discharge into inland sinks was included.

No. Component GSWP3 PGFv2 WFD WFDEI_hom WFD_WFDEI

1 Precipitation P (km3 yr1) 109 631 103 525 110 690 111 050 111 050

2 Actual evapotranspiration AETa 62.0 61.3 61.1 63.0 62.0

3 Discharge into oceans and inland sinks Qb 37.1 37.8 38.1 36.2 37.2

4 Water consumption (actual) WCa 0.9 0.9 0.8 0.9 0.8

5 Change of total water storage dS / dtc 0.01 0.03 0.02 0.02 0.07

a AET does not include evapotranspiration caused by human water use, i.e. actual water consumption WCa. b Taking into account anthropogenic water use.

c Total water storage (TWS) of 31 December 2000 minus TWS of 31 December 1970, divided by the number of 30 years.

2.5 % of precipitation is evapotranspired, mainly due to irrigation. For the other continents, water consumption plays relative to the other water balance components only a marginal role. The lowest runoff coefcient (Q/P ) is found in Africa (0.21), whereas runoff coefcients vary between0.34 (Oceania) and 0.47 (Europe) for the other continents.

Hence, differences in P result in higher relative uncertainties of estimated water resources for Africa. The deviation from the mean continental value for Q among the climate forcings is between 5.9 (calculated as min Q / mean Q) and 10.9 %

(max Q / mean Q) for Africa, whereas for all other continents deviations are lower (5.4 and 2.2 as minimum Q,

2.55.0 % as maximum Q).

3.3 Global water balance components

Compared to the continental-scale deviation of water balance components, the impact of climate forcing uncertainty

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creased, LWD is decreased (and vice versa), which reduces the effect on net radiation. T effects model results via the equation for potential evapotranspiration (Priestley and Taylor, 1972), via snow dynamics as well as the leaf area index model that affects canopy evaporation (details in Mller Schmied et al., 2014). As T differs only little between the forcing datasets (Fig. A2), effects of T differences on simulated net cell runoff are expected to be relatively small.

3.2 Continental water balance components

Figure 2 displays the continental-scale partitioning of precipitation into actual evapotranspiration AET, river discharge Q, and human water consumption WCa. South America and Africa have nearly the same absolute amount of AET, but values for Q differ strongly. As a consequence of extensive irrigated agriculture especially in India and China (Siebert et al., 2015), the highest water consumption occurs in Asia, where

H. Mller Schmied et al.: Impact of climate forcing uncertainty and human water use 57

Figure 3. Development of water abstractions (sum of return ows and consumptive use) and water consumption (the amount of water that is evapotranspired or incorporated in products, light colours) of the ve water use sectors considered in WaterGAP for 19012010. Values for irrigation (modelled with 70 % of demand in grid cells with groundwater depletion) are averaged across the ve climate forcings; other sectors are modelled independently of climate forcing and taken from Flrke et al. (2013).

is levelling out at the global scale to a certain degree (Table 2). Global runoff coefcients vary between 0.362 and0.381, and deviation of global Q from the ensemble mean is 3.8 to 3.7 %. Actual evapotranspiration is estimated to

range between 61.1 and 63.0 % of global P (Table 2). The lowest value for AET (and highest value for Q) is computed when using WFD climate forcing. Here, average global SWD is 15 W m2 lower compared to the other forcings (see also Mller Schmied et al., 2016, their Fig. 1). In absolute numbers, differences in AET and Q resulting from the ve climate forcings are considerable. For example, global discharge values range from 39 200 to 42 200 km3 yr1: the uncertainty range is equal to thrice the total water consumption ( 930 km3 yr1).

On the global scale, sectoral water uses have strongly increased since 1901 (Fig. 3). Whereas overall water abstractions (consumptive use) are about 650 (260) km3 yr1 in the year 1901, values are about 5 times higher with 3700 (1250) km3 yr1 in 2010. In contrast to Mller Schmied et al. (2016, their Fig. 1), where water consumption of each climate forcing is presented using different time step aggregations, Fig. 3 shows the proportion of potential (if water were available without limitation) consumptive water use components (light colours) and the amount of return ows (dark colours). The most important water use sector regarding both abstraction and consumption is the irrigation sector. The sum of potential water consumption of all water use sectors (except irrigation) throughout the period 19712000 is 112 km3 yr1, whereas the sums of potential irrigation water consumption vary between 834 and 894 km3 yr1 depend-

ing on the climate forcings. Together with the other potential water uses (manufacturing, cooling of thermal power plants, domestic and livestock sector), the demand of consumptive water uses ranges from 946 to 1006 km3 yr1. Due to limited water availability to satisfy the demand, actual water consumption (WCa) ranges between 915 (WFD) and 960 (PGFv2) km3 yr1 (all numbers 19712000). Hence, water availability reduces the impact of climate forcing uncertainty when modelling water use demand. The uncertainty range of estimated global irrigation water consumption due to the climate forcing is therefore about 50 % of the sum of all the other water use sectors.

4 Conclusions

Within this study, the WaterGAP 2.2 (ISIMIP2a) model was used to assess water balance components on grid-cell, continental and global scale as well as the development of human water use on the global scale. The research questions can be answered as follows:

1. How does climate forcing affect computed runoff at the grid-cell level?

On the grid-cell level, the effect of climate forcing uncertainty on computed runoff is very large. In particular, usage of different observation-based products to bias-correct reanalysis data affects the spatial distribution of runoff. Furthermore, undercatch correction (or the lack thereof) of P leads to differences in model estimates. Whereas T uncertainty does not lead to clearly visible spatial differences in computed runoff, SWD uncertainty was found to have a large impact in energy-limited regions like tropical Africa. For water-limited areas, this is not the case.

2. How does climate forcing uncertainty and human water use affect long-term average water balance components on global and continental scales?

Climate forcing uncertainty is high (Figs. A1A4), and most important are differences in P and SWD. At the continental scale, these uncertainties lead to large differences in calculated water balance components, in particular in regions with high P uncertainty and low runoff coefcient (e.g. Africa).Global-scale values vary less in relative terms as deviations even out with spatial aggregation. The uncertainty range of estimated global irrigation water consumption due to uncertain climate forcing is around 50 % of the water consumption in the other water use sectors.

Multi-model hydrological assessments as done by the ISIMIP initiative for both historical periods (e.g. Haddeland et al., 2011) and future scenarios (e.g. Schewe et al., 2014) will help to relate the uncertainties of water balance components at different scales of aggregation that are caused by different climate forcings to uncertainties due to the hydro-logical models themselves. To constrain both types of uncertainty, model calibration not only of mean annual river

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58 H. Mller Schmied et al.: Impact of climate forcing uncertainty and human water use

discharge (as done for the WaterGAP model) but also of remote-sensing-based data like total water storage variations from GRACE (Eicker et al., 2014; Dll et al., 2014b, 2016) is promising, but collection and sharing of in situ data remains crucial (Fekete et al., 2015).

5 Data availability

The WaterGAP output will become freely available to the public within the framework of the ISIMIP project phase 2a, but it is not yet claried where the data will be hosted (please check https://www.isimip.org/outputdata/

Web End =https://www.isimip.org/outputdata/ for updates). The homogenized climate forcing WFDEI_hom is not included within the ISI-MIP project. All model outputs used in this study are available on request from the corresponding author.

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H. Mller Schmied et al.: Impact of climate forcing uncertainty and human water use 59

Appendix A

Figure A1. Long-term (19712000) average precipitation of the model variants, displayed as absolute number for GSWP3 (a) and differences to the other forcings, computed as PGFv2 minus GSWP3 (b), WFD minus GSWP3 (c), WFD_WFDEI minus GSWP3 (d), and WFDEI_hom minus GSWP3 (e). All units in mm yr1.

Figure A2. Long-term (19712000) average temperature of the model variants, displayed as absolute number for GSWP3 (a) and differences to the other forcings, computed as PGFv2 minus GSWP3 (b), WFD minus GSWP3 (c), WFD_WFDEI minus GSWP3 (d), and WFDEI_hom minus GSWP3 (e). All units in C.

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60 H. Mller Schmied et al.: Impact of climate forcing uncertainty and human water use

Figure A3. Long-term (19712000) average shortwave downward radiation of the model variants, displayed as absolute number for GSWP3 (a) and differences to the other forcings, computed as PGFv2 minus GSWP3 (b), WFD minus GSWP3 (c), WFD_WFDEI minus GSWP3 (d), and WFDEI_hom minus GSWP3 (e). All units in W m2.

Figure A4. Long-term (19712000) average longwave downward radiation of the model variants, displayed as absolute number for GSWP3 (a) and differences to the other forcings, computed as PGFv2 minus GSWP3 (b), WFD minus GSWP3 (c), WFD_WFDEI minus GSWP3 (d), and WFDEI_hom minus GSWP3 (e). All units in W m2.

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H. Mller Schmied et al.: Impact of climate forcing uncertainty and human water use 61

Acknowledgements. The authors thank the Global Runoff Data Centre (GRDC, http://grdc.bafg.de

Web End =http://grdc.bafg.de ), 56068 Koblenz, Germany, for providing the discharge data used in this study for calibrating the model. We are also grateful to the ISI-MIP coordination team as well as the leaders of the water sector (Simon Gosling and Rutger Dankers) for providing the climate forcings and the support. Furthermore, we thank Wolfgang Grabs for organizing the international conference Water Resources Assessment & Seasonal Prediction (1316 October in Koblenz, Germany), where some content of this paper was presented.

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