# Intercomparison of Solid Precipitation Derived from the Weighting Rain Gauge and Optical Instruments in the Interior Qinghai-Tibetan Plateau

Authors: Lele Zhang; Lin Zhao; Changwei Xie; Guangyue Liu; Liming Gao; Yao Xiao; Jianzong Shi; Yongping Qiao
Journal: Advances in Meteorology
 (2015)

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## Abstract

Due to the light precipitation and strong wind in the cold season, it is hard to get credible solid precipitation on the Qinghai-Tibetan plateau (QTP). To address this issue, two kinds of optical instruments, the Thies Laser Precipitation Monitor (LPM) and OTT laser-optical Particle Size Velocity (Parsivel), were used on QTP. The measured precipitation was compared with the precipitation derived from Geonor T-200B precipitation gauge (Geonor). The results showed that Geonor was hard to catch light precipitation (precipitation amount was less than 1 mm during a single event) when the wind speeds were higher than 3.5 m/s. Even when the wind speeds were smaller than 3.5 m/s, about 44% of such light precipitation events were not recorded by Geonor. The optical instruments had much better performance in recording light precipitation. Three methods were used to correct Geonor measurements of daily solid precipitation and the corrected values were set as reference for assessing the performance of LPM and Parsivel; the results showed that LPM had good performance in measuring the solid precipitation but Parsivel overestimated the precipitation amount. Methods for correcting Geonor’s hourly solid precipitation and recalculating Parsivel’s solid precipitation amount were also proposed in this paper.


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## Body

## 1. Introduction

Accurate precipitation is important for better understanding the climate change and water cycle [1–4], and it is also a crucial component of hydrologic and climatologic models [4–6]. Currently, the precipitation is mainly measured by different kinds of rain gauges; however, it is generally recognized that the gauge-measured precipitation has systematic errors including wetting, evaporation losses, and wind-induced undercatch [7–9]. Especially the solid precipitation, the measurement errors frequently range from 20% to 50% due to undercatch in windy conditions [10]. In order to get the true solid precipitation, the World Meteorological Organization (WMO) carried out a series of programs. In the third WMO precipitation measurement intercomparison (1986–1993), the Double Fence International Reference (DFIR) with a shielded Tretyakov gauge was designated as the reference standard snow gauges [11]. Since 2012, the WMO Commission for Instruments and Methods of Observation organized the Solid Precipitation Intercomparison Experiment (SPICE); the main objectives of the project are to define and validate the field references for gauge intercomparison and to assess the automatic systems used in the operational networks for solid precipitation observations [12]. Under these projects, the gauge undercatch of solid precipitation had greatly improved in most areas of the global. In China, Ye et al. [13] corrected the precipitation data over China and reported an approximately 16% increase in mean yearly precipitation during 1951–2004. Ding et al. [14] compared the measured and corrected precipitation data over China during 1951–1998 and found that bias corrections of precipitation lead to an 8% overall enhancement of yearly precipitation trends over China. Ma et al. [15] corrected the precipitation data by using different kinds of error correction procedures in the Third Pole Environment (TPE) region and found that the average annual precipitation has increased from a minimum of 4 mm to a maximum of 409 mm in this region. However, no special attention had been paid on the solid precipitation correction in the interior QTP until now [16].QTP is known for its large sensible and latent heating effects on the troposphere over Asia. Quantitative evaluation of area precipitation is one of the important aspects for estimating latent heating and understanding the water cycle processes over this unique highland [17]. Compared with the other regions, the climate in the interior of QTP is special; the wind is strong and the light precipitation is dominant in winter, and the manual observation is unrealistic during this period due to the severe weather conditions, so it is nearly impossible to obtain the light solid precipitation from the traditional rain gauges.Sugiura et al. [8] first introduced a snow particle counter (SPC) to solid precipitation measurement and proposed that the optical instruments like SPC should be used in solid precipitation measurements in the Arctic. Compared with SPC, LPM and Parsivel are kinds of more mature optical products and were well tested in liquid precipitation measurements before [18–21]. Furthermore, both of LPM and Parsivel had been used by the WMO for solid precipitation measurement in the SPICE project. Because LPM and Parsivel use the light beam for precipitation monitoring, the wind-induced precipitation will be much smaller. Furthermore, the minimum precipitation intensity derived from the LPM and Parsivel is 0.005 mm/h and 0.001 mm/h, respectively; it seems that the optical instruments will be most suitable for solid precipitation measurement in the interior QTB. However, no attention had been paid to whether they can be used for the solid precipitation observation in these regions until now.In this study, we analyzed solid precipitation derived from Geonor and two kinds of optical instruments (Parsivel and LPM) at three meteorological stations in the Beiluhe (BLH), Tanggula (TGL), and Wudaoliang (WDL) lie in the interior QTP. Considering the old version of Parsivel has large error when measuring snow [22], the two Parsivel instruments used in this study are the latest version (Parsivel2). Our goals are (1) investigating Geonor’s deficiency in recording the light solid precipitation and (2) assessing the performance of optical instruments in measuring the solid precipitation in the interior QTP. Finally, we hope to get the more reliable solid precipitation data in these regions.The paper is organized as follows. Section2 introduces the basic conditions and the instruments in the study sites; the correcting methods for Geonor’s daily solid precipitation are also introduced in this section. Section 3 compares the solid precipitation derived from the different instruments and the performance of Geonor in recording light precipitation is also discussed in this section. In Section 4, a statistic method for determining Parsivel’s snow particles diameter correction factor (α) is proposed and the Parsivel solid precipitation amounts are recalculated. The discussions and conclusions are in Section 5.


## 2. Methodology

### 2.1. Study Sites

The observation stations chosen in this study are Beiluhe (BLH; 92.9°E, 34.8°N, 4600 m above sea level), Tanggula (TGL; 91.9°E, 33.1°N, 5100 m above sea level), and Wudaoliang (WDL; 93.1°E, 35.2°N, 4783 m above sea level). All of the three stations are located in the interior QTP (Figure1). Based on previous observations, the mean annual air temperature (MAAT) in BLH is −3.8°C, with the highest value of 21.3°C in mid-July and lowest value of −21.4°C in later January [23, 24]. In TGL station, the MAAT is about −4.1°C and its highest and lowest values are 16.2°C and −30.5°C [25]. The MAAT in WDL is about −5.1°C and maximum and minimum air temperature are 20.1°C and −26.5°C [26]. The mean annual precipitation in the three stations are 368 mm, 436.7 mm, and 294.8 mm, respectively [26, 27]. Due to the summer monsoon generally occurring from May to October, the precipitation events on the QTP mainly occur during the period from June to September. Like most areas on the QTP, the cold season of the three stations is long and the wind speeds during this periods are large, the instantaneous wind speed can reach to larger than 15 m/s.Figure 1
Location of the observation site and precipitation observation devices. (a) BLH, (b) TGL, and (c) WDL.In the three stations, the routine meteorological parameters like wind (2 m, 5 m, and 10 m), air temperature (2 m, 5 m, and 10 m), humidity (2 m, 5 m, and 10 m), precipitation, and solar radiation had been monitored since the early 21st century. The rain gauge used in the TGL and WDL stations is Geonor, but in the BLH station is TE525 tipping-bucket rain gauge. In order to get the more detailed and accurate precipitation information, a LPM and a Geonor precipitation gauge were set in the BLH station in 2011 and 2012 separately. In the end of 2014, two Parsivel instruments had been installed in the TGL and WDL stations. In this study, the Geonor precipitation data were recorded every one hour in BLH station and every 30 minutes in TGL and WDL stations. In order to understand the microscopic information of the precipitation, the LPM and Parsivel data were recorded every minute. All of the data were logged by the CR23X or CR3000 data logger (Campbell Scientific Inc.).


### 2.2. Introduction of Instruments

The LPM uses the light beam for precipitation monitoring. Every time when precipitation particles pass through the sensing volume, it is capable of measuring their diameter and falling velocity [20]. From these measurements, it identifies the type of precipitation and calculates precipitation rate, drop-size distribution, and some other parameters. Bloemink and Lanzinger [18] compared the precipitation type derived from LPM with the Vaisala FD12P Present Weather Sensor and proposed the LPM can identify the precipitation accurately.OTT Parsivel is also a laser-based optical disdrometer for simultaneously measuring the size and velocity of all types of hydrometeors during precipitation [21]. Its operating principle is similar to LPM, and the measurement area is 54 cm2, a little larger than LPM. The sensor determines the size and velocity of a hydrometeor by measuring the light extinction caused by the hydrometeor falling through the light sheet. The hydrometeor is then classified into 32 classes of sizes and velocity. From the size and velocity distribution information over the measurement period, the precipitation type, rate, and amount are determined.Geonor is an automated weighing storage gauge which is widely used in the interior QTP. It continuously measures the weight of accumulated snowfall in a reservoir containing antifreeze solution and oil which melt the snow and reduce evaporation. The reservoir is suspended on a wire strain gauge which vibrates at a frequency proportional to the applied strain. The reservoir and strain gauge are in a protective housing which is surrounded by the Alter-shield. The Geonor has a resolution of 0.1 mm SWE and an accuracy of 0.1% [28].


### 2.3. Methods for Correcting Geonor Solid Precipitation

Geonor is widely used in the Arctic and QTP regions. Like the other precipitation gauges, Geonor’s catch efficiency (CE) is also highly affected by the wind. Many scholars had proposed the correction methods for Geonor; the widely used correction methods were proposed by Smith [29] and MacDonald and Pomeroy [30]:(1)CEGeonor=PGeonorPDFIR=exp⁡-0.2WS,(2)CEGeonor=PGeonorPc-Nipher=1.01exp⁡-0.09WS.Equation (1) was proposed by Smith and (2) was by MacDonald and Pomeroy. Both of the two methods had been widely used and proven effective in improving the hydrological simulation [31–36].In the interior QTP, Zhao et al. [37] had also proposed the correction formula:(3)CEGeonor=PGeonorPc-CSPG=exp⁡-0.135WS.In the equations above, CEGeonor is solid precipitation catch efficiency of Geonor, PGeonor is the daily precipitation recorded by Geonor, PDFIR is precipitation recorded by the double fence intercomparison reference (DFIR), and Pc-Nipher and Pc-CSPG are precipitation from corrected Nipher and Chinese standard precipitation gauge (CSPG), respectively. Adjustment procedures for Nipher and CSPG rain gauge had been developed by the WMO [38, 39]. WS is the wind speed at gauge height measured in m/s. In BLH, there is a wind speed sensor at the gauge height. In the TGL and WDL, the wind speeds at the gauge height are calculated by using data at 2 m height based on the method proposed by Zhao et al. [37]:(4)WS=lg⁡h/z0lg⁡H/z0WS2m,where WS is the wind speed at the gauge height, h is the gauge height (m), z0 is surface roughness (m), He et al. [28] and Zhao et al. [37] set z0 as 0.01 m in cold season in the interior QTP, H is the wind sensor installed height (2 m in this study), and WS2m is the wind speed at 2 m height.The formulas (1)–(3) assume the DFIR as the “true” precipitation substantially. Yang [12] compared the precipitation derived from DFIR and the Bush Gauge and found that the Bush Gauge measures 20–50% more snow than the DFIR for wind speeds of 6-7 m/s. He also proposed the correction methods for DFIR. For dry snow, the formula is as follows:(5)PBushPDFIR=100+0.171WS2+0.2WS.


## 2.1. Study Sites

The observation stations chosen in this study are Beiluhe (BLH; 92.9°E, 34.8°N, 4600 m above sea level), Tanggula (TGL; 91.9°E, 33.1°N, 5100 m above sea level), and Wudaoliang (WDL; 93.1°E, 35.2°N, 4783 m above sea level). All of the three stations are located in the interior QTP (Figure1). Based on previous observations, the mean annual air temperature (MAAT) in BLH is −3.8°C, with the highest value of 21.3°C in mid-July and lowest value of −21.4°C in later January [23, 24]. In TGL station, the MAAT is about −4.1°C and its highest and lowest values are 16.2°C and −30.5°C [25]. The MAAT in WDL is about −5.1°C and maximum and minimum air temperature are 20.1°C and −26.5°C [26]. The mean annual precipitation in the three stations are 368 mm, 436.7 mm, and 294.8 mm, respectively [26, 27]. Due to the summer monsoon generally occurring from May to October, the precipitation events on the QTP mainly occur during the period from June to September. Like most areas on the QTP, the cold season of the three stations is long and the wind speeds during this periods are large, the instantaneous wind speed can reach to larger than 15 m/s.Figure 1
Location of the observation site and precipitation observation devices. (a) BLH, (b) TGL, and (c) WDL.In the three stations, the routine meteorological parameters like wind (2 m, 5 m, and 10 m), air temperature (2 m, 5 m, and 10 m), humidity (2 m, 5 m, and 10 m), precipitation, and solar radiation had been monitored since the early 21st century. The rain gauge used in the TGL and WDL stations is Geonor, but in the BLH station is TE525 tipping-bucket rain gauge. In order to get the more detailed and accurate precipitation information, a LPM and a Geonor precipitation gauge were set in the BLH station in 2011 and 2012 separately. In the end of 2014, two Parsivel instruments had been installed in the TGL and WDL stations. In this study, the Geonor precipitation data were recorded every one hour in BLH station and every 30 minutes in TGL and WDL stations. In order to understand the microscopic information of the precipitation, the LPM and Parsivel data were recorded every minute. All of the data were logged by the CR23X or CR3000 data logger (Campbell Scientific Inc.).


## 2.2. Introduction of Instruments

The LPM uses the light beam for precipitation monitoring. Every time when precipitation particles pass through the sensing volume, it is capable of measuring their diameter and falling velocity [20]. From these measurements, it identifies the type of precipitation and calculates precipitation rate, drop-size distribution, and some other parameters. Bloemink and Lanzinger [18] compared the precipitation type derived from LPM with the Vaisala FD12P Present Weather Sensor and proposed the LPM can identify the precipitation accurately.OTT Parsivel is also a laser-based optical disdrometer for simultaneously measuring the size and velocity of all types of hydrometeors during precipitation [21]. Its operating principle is similar to LPM, and the measurement area is 54 cm2, a little larger than LPM. The sensor determines the size and velocity of a hydrometeor by measuring the light extinction caused by the hydrometeor falling through the light sheet. The hydrometeor is then classified into 32 classes of sizes and velocity. From the size and velocity distribution information over the measurement period, the precipitation type, rate, and amount are determined.Geonor is an automated weighing storage gauge which is widely used in the interior QTP. It continuously measures the weight of accumulated snowfall in a reservoir containing antifreeze solution and oil which melt the snow and reduce evaporation. The reservoir is suspended on a wire strain gauge which vibrates at a frequency proportional to the applied strain. The reservoir and strain gauge are in a protective housing which is surrounded by the Alter-shield. The Geonor has a resolution of 0.1 mm SWE and an accuracy of 0.1% [28].


## 2.3. Methods for Correcting Geonor Solid Precipitation

Geonor is widely used in the Arctic and QTP regions. Like the other precipitation gauges, Geonor’s catch efficiency (CE) is also highly affected by the wind. Many scholars had proposed the correction methods for Geonor; the widely used correction methods were proposed by Smith [29] and MacDonald and Pomeroy [30]:(1)CEGeonor=PGeonorPDFIR=exp⁡-0.2WS,(2)CEGeonor=PGeonorPc-Nipher=1.01exp⁡-0.09WS.Equation (1) was proposed by Smith and (2) was by MacDonald and Pomeroy. Both of the two methods had been widely used and proven effective in improving the hydrological simulation [31–36].In the interior QTP, Zhao et al. [37] had also proposed the correction formula:(3)CEGeonor=PGeonorPc-CSPG=exp⁡-0.135WS.In the equations above, CEGeonor is solid precipitation catch efficiency of Geonor, PGeonor is the daily precipitation recorded by Geonor, PDFIR is precipitation recorded by the double fence intercomparison reference (DFIR), and Pc-Nipher and Pc-CSPG are precipitation from corrected Nipher and Chinese standard precipitation gauge (CSPG), respectively. Adjustment procedures for Nipher and CSPG rain gauge had been developed by the WMO [38, 39]. WS is the wind speed at gauge height measured in m/s. In BLH, there is a wind speed sensor at the gauge height. In the TGL and WDL, the wind speeds at the gauge height are calculated by using data at 2 m height based on the method proposed by Zhao et al. [37]:(4)WS=lg⁡h/z0lg⁡H/z0WS2m,where WS is the wind speed at the gauge height, h is the gauge height (m), z0 is surface roughness (m), He et al. [28] and Zhao et al. [37] set z0 as 0.01 m in cold season in the interior QTP, H is the wind sensor installed height (2 m in this study), and WS2m is the wind speed at 2 m height.The formulas (1)–(3) assume the DFIR as the “true” precipitation substantially. Yang [12] compared the precipitation derived from DFIR and the Bush Gauge and found that the Bush Gauge measures 20–50% more snow than the DFIR for wind speeds of 6-7 m/s. He also proposed the correction methods for DFIR. For dry snow, the formula is as follows:(5)PBushPDFIR=100+0.171WS2+0.2WS.


## 3. Results

### 3.1. Overview of Data

In the BLH station, observations were carried out from 2011/11/11 to 2012/4/30 and from 2012/11/1 to 2013/5/16. During the first period, the Geonor precipitation gauge was not installed in the BLH site; Geonor precipitation data were obtained from a meteorological station nearby (set by the State Key Laboratory of Frozen Soil Engineering, Cold and Arid Regions Environmental and Engineering Research Institute, Chinese Academy of Sciences, less than 1 km far from our site). During the second period, 33 days were not observed for the power supply reason. In TGL and WDL stations, the Parsivel instruments worked very well after installation and the data were collected every two months; the data of the two stations used in this study were from 2014/10/1 to 2015/4/30 and from 2014/10/1 to 2015/2/3, respectively. During the study periods, the winds were strong and the instantaneous wind speed can reach to larger than 10 m/s in BLH and 16 m/s in TGL (Figure2). Due to the high frequency light precipitation and the strong wind, processing solid precipitation data from Geonor precipitation gauge was also hard work. In this study, we processed the data carefully and used the optical instruments data as the standard for the judgment of precipitation events.Figure 2
Wind speed during the study periods in (a) BLH and (b) TGL stations.
(a)
(b)During the study periods, the precipitation days recorded by Geonor and the optical instruments were different (Figure3). In the BLH station, LPM recorded 79 and 47 precipitation days during the two periods, but Geonor only recorded 31 and 27 precipitation days. In the TGL station, the precipitation days were 45 and 80 recorded by Geonor and Parsivel, respectively. In the WDL station, Parsivel recorded 41 while Geonor only recorded 18 precipitation days. In order to find which instrument was more credible, we chose a precipitation event during 2014/11/2 in TGL station (Figure 4); the Parsivel recorded 4.44 mm precipitation while the Geonor recorded no precipitation. By comparing the radiation and albedo with the before and the proceeding day, we found that both the global and net radiation decreased on November 2, and the albedo increased in the afternoon. The results showed that it was a precipitation day on 2014/11/2. This indicates that the optical instruments can record light precipitation that cannot be recorded by the Geonor.Figure 3
Precipitation days recorded by different instruments (a) from 2011/11/11 to 2012/4/30 and (b) from 2012/11/1 to 2013/5/16 in BLH, (c) from 2014/10/1 to 2015/4/30 in TGL, and (d) from 2014/10/1 to 2015/4/3 in WDL.
(a)
(b)
(c)
(d)Figure 4
Variation of the (a) global and net radiation and (b) albedo during a single precipitation event.
(a)
(b)


### 3.2. Comparison of the Daily Solid Precipitation

The precipitation types recorded by LPM and Parsivel in the interior QTP were very complex in May and September, including drizzle, rain, snow, wet snow, sleet, freezing rain, hail, and mixed precipitation. When the precipitation type was wet snow or sleet, the optical instruments recorded abnormal large precipitation amount; this is because the wet snow particles are easier to agglutinate, and both LPM and Parsivel use the equivalent diameter for calculating the precipitation; the agglutinated particles will increase the observation errors. In this study, we removed the wet snow precipitation days when comparing the daily solid precipitation. In BLH station, all of the three methods introduced in Section2.3 were used to correct the precipitation recorded by Geonor, and the corrected precipitation was compared with the precipitation recorded by LPM (Figure 5). It was shown in Figure 5(a) that the daily precipitation measured by Geonor (PGeonor) was smaller than LPM (PLPM). After correction by the three methods, the precipitation measured by Geonor was in good agreement with PLPM (Figures 5(b), 5(c), and 5(d)). The mean absolute error (MAE) was used for assessing the consistency between daily PLPM and the corrected Geonor based on the three methods:(6)MAE=1n∑i=1nPLPMi-Pc-Geonori,where n is the sample size, PLPM is the daily precipitation recorded by LPM (mm), and Pc-Geonor is the corrected Geonor precipitation (mm). The results showed that the daily PLPM are in best agreement with PGeonor corrected by Smith’s method with the MAE=0.47 mm.Figure 5
Comparing the daily solid precipitation derived from LPM with (a) Geonor’s original precipitation; corrected precipitation by methods proposed by (b) Smith, (c) MacDonald and Pomeroy, and (d) Zhao et al. in the BLH station.
(a)
(b)
(c)
(d)The scattergram of daily corrected Geonor precipitation (Pc-Geonor) and precipitation recorded by Parsivel (PParsivel) in TGL station were shown in Figure 6; the daily Pc-Geonor by the three correction methods were still much smaller than PParsivel. Furthermore, the precipitation amount during 2014/10/1 and 2015/4/30 in TGL station recorded by Parsivel was 305 mm; this disagrees with the reality of the interior QTP. Therefore, we proposed that the Parsivel overestimated the solid precipitation in these regions. Boudala et al. [40] compared the solid precipitation rate and the total precipitation derived from three instruments (Pluvio, Parsivel, and PD12P) on Whistler Mountain in Canada and also proposed that the Parsivel overestimated the solid precipitation, which is consistent with the conclusion in our study.Figure 6
Comparing the daily solid precipitation derived from Parsivel with Geonor’s original and corrected precipitation in TGL station.


### 3.3. Assessing Geonor’s Deficiency in Recording Light Solid Precipitation

The precipitation gauge includes the DFIR which cannot detect the light solid precipitation under the wind conditions [8]. In this section, Geonor’s deficiency in recording light solid precipitation in the interior QTP had also been investigated. 75 precipitation events at different precipitation amount and wind speed recorded by LPM were used for finding the light precipitation threshold that can be detected by the Geonor. It can be seen from Figure 7 that when the wind speeds (WS) were larger than 3.5 m/s, the Geonor nearly could not record the precipitation events when the amount was smaller than 1 mm. Even when 0.5 < WS < 3.5 m/s, about 44% of these light precipitation still could not be recorded by Geonor.Figure 7
Precipitation threshold that can be detected by the Geonor under different wind conditions.


### 3.4. Correcting Geonor’s Hourly Solid Precipitation

In some of the meteorological and hydrological fields, daily precipitation data are far from perfect for subdaily research. Correcting the hourly solid precipitation is also necessary in the interior QTP. When correcting the gauge measurements of daily solid precipitation, it is generally believed that the catch efficiency (CE) of the precipitation gauge has an exponential relationship with the wind speed. In this study, we took the LPM precipitation as the reference values and calculated the hourly CE of Geonor(CEGeonor). The exponential function was chosen for fitting the relationship between the wind speed at gauge height (WS) and CEGeonor (Figure 8; only both hourly PGeonor and PLPM larger than 0.5 mm are used):(7)CEGeonor=PGeonorPLPM=1.017exp⁡-0.22WS.Figure 8
Relationship between the hourlyPGeonor/PLPM and the wind speed (WS).The regression is statistically significance withF value = 96.8 and α<0.01 by using the F test. However, it is important to note that the data are scattered. One possible explanation is that the frequency of light precipitation is high in these regions; the Geonor has large system errors when recording the light precipitation.


## 3.1. Overview of Data

In the BLH station, observations were carried out from 2011/11/11 to 2012/4/30 and from 2012/11/1 to 2013/5/16. During the first period, the Geonor precipitation gauge was not installed in the BLH site; Geonor precipitation data were obtained from a meteorological station nearby (set by the State Key Laboratory of Frozen Soil Engineering, Cold and Arid Regions Environmental and Engineering Research Institute, Chinese Academy of Sciences, less than 1 km far from our site). During the second period, 33 days were not observed for the power supply reason. In TGL and WDL stations, the Parsivel instruments worked very well after installation and the data were collected every two months; the data of the two stations used in this study were from 2014/10/1 to 2015/4/30 and from 2014/10/1 to 2015/2/3, respectively. During the study periods, the winds were strong and the instantaneous wind speed can reach to larger than 10 m/s in BLH and 16 m/s in TGL (Figure2). Due to the high frequency light precipitation and the strong wind, processing solid precipitation data from Geonor precipitation gauge was also hard work. In this study, we processed the data carefully and used the optical instruments data as the standard for the judgment of precipitation events.Figure 2
Wind speed during the study periods in (a) BLH and (b) TGL stations.
(a)
(b)During the study periods, the precipitation days recorded by Geonor and the optical instruments were different (Figure3). In the BLH station, LPM recorded 79 and 47 precipitation days during the two periods, but Geonor only recorded 31 and 27 precipitation days. In the TGL station, the precipitation days were 45 and 80 recorded by Geonor and Parsivel, respectively. In the WDL station, Parsivel recorded 41 while Geonor only recorded 18 precipitation days. In order to find which instrument was more credible, we chose a precipitation event during 2014/11/2 in TGL station (Figure 4); the Parsivel recorded 4.44 mm precipitation while the Geonor recorded no precipitation. By comparing the radiation and albedo with the before and the proceeding day, we found that both the global and net radiation decreased on November 2, and the albedo increased in the afternoon. The results showed that it was a precipitation day on 2014/11/2. This indicates that the optical instruments can record light precipitation that cannot be recorded by the Geonor.Figure 3
Precipitation days recorded by different instruments (a) from 2011/11/11 to 2012/4/30 and (b) from 2012/11/1 to 2013/5/16 in BLH, (c) from 2014/10/1 to 2015/4/30 in TGL, and (d) from 2014/10/1 to 2015/4/3 in WDL.
(a)
(b)
(c)
(d)Figure 4
Variation of the (a) global and net radiation and (b) albedo during a single precipitation event.
(a)
(b)


## 3.2. Comparison of the Daily Solid Precipitation

The precipitation types recorded by LPM and Parsivel in the interior QTP were very complex in May and September, including drizzle, rain, snow, wet snow, sleet, freezing rain, hail, and mixed precipitation. When the precipitation type was wet snow or sleet, the optical instruments recorded abnormal large precipitation amount; this is because the wet snow particles are easier to agglutinate, and both LPM and Parsivel use the equivalent diameter for calculating the precipitation; the agglutinated particles will increase the observation errors. In this study, we removed the wet snow precipitation days when comparing the daily solid precipitation. In BLH station, all of the three methods introduced in Section2.3 were used to correct the precipitation recorded by Geonor, and the corrected precipitation was compared with the precipitation recorded by LPM (Figure 5). It was shown in Figure 5(a) that the daily precipitation measured by Geonor (PGeonor) was smaller than LPM (PLPM). After correction by the three methods, the precipitation measured by Geonor was in good agreement with PLPM (Figures 5(b), 5(c), and 5(d)). The mean absolute error (MAE) was used for assessing the consistency between daily PLPM and the corrected Geonor based on the three methods:(6)MAE=1n∑i=1nPLPMi-Pc-Geonori,where n is the sample size, PLPM is the daily precipitation recorded by LPM (mm), and Pc-Geonor is the corrected Geonor precipitation (mm). The results showed that the daily PLPM are in best agreement with PGeonor corrected by Smith’s method with the MAE=0.47 mm.Figure 5
Comparing the daily solid precipitation derived from LPM with (a) Geonor’s original precipitation; corrected precipitation by methods proposed by (b) Smith, (c) MacDonald and Pomeroy, and (d) Zhao et al. in the BLH station.
(a)
(b)
(c)
(d)The scattergram of daily corrected Geonor precipitation (Pc-Geonor) and precipitation recorded by Parsivel (PParsivel) in TGL station were shown in Figure 6; the daily Pc-Geonor by the three correction methods were still much smaller than PParsivel. Furthermore, the precipitation amount during 2014/10/1 and 2015/4/30 in TGL station recorded by Parsivel was 305 mm; this disagrees with the reality of the interior QTP. Therefore, we proposed that the Parsivel overestimated the solid precipitation in these regions. Boudala et al. [40] compared the solid precipitation rate and the total precipitation derived from three instruments (Pluvio, Parsivel, and PD12P) on Whistler Mountain in Canada and also proposed that the Parsivel overestimated the solid precipitation, which is consistent with the conclusion in our study.Figure 6
Comparing the daily solid precipitation derived from Parsivel with Geonor’s original and corrected precipitation in TGL station.


## 3.3. Assessing Geonor’s Deficiency in Recording Light Solid Precipitation

The precipitation gauge includes the DFIR which cannot detect the light solid precipitation under the wind conditions [8]. In this section, Geonor’s deficiency in recording light solid precipitation in the interior QTP had also been investigated. 75 precipitation events at different precipitation amount and wind speed recorded by LPM were used for finding the light precipitation threshold that can be detected by the Geonor. It can be seen from Figure 7 that when the wind speeds (WS) were larger than 3.5 m/s, the Geonor nearly could not record the precipitation events when the amount was smaller than 1 mm. Even when 0.5 < WS < 3.5 m/s, about 44% of these light precipitation still could not be recorded by Geonor.Figure 7
Precipitation threshold that can be detected by the Geonor under different wind conditions.


## 3.4. Correcting Geonor’s Hourly Solid Precipitation

In some of the meteorological and hydrological fields, daily precipitation data are far from perfect for subdaily research. Correcting the hourly solid precipitation is also necessary in the interior QTP. When correcting the gauge measurements of daily solid precipitation, it is generally believed that the catch efficiency (CE) of the precipitation gauge has an exponential relationship with the wind speed. In this study, we took the LPM precipitation as the reference values and calculated the hourly CE of Geonor(CEGeonor). The exponential function was chosen for fitting the relationship between the wind speed at gauge height (WS) and CEGeonor (Figure 8; only both hourly PGeonor and PLPM larger than 0.5 mm are used):(7)CEGeonor=PGeonorPLPM=1.017exp⁡-0.22WS.Figure 8
Relationship between the hourlyPGeonor/PLPM and the wind speed (WS).The regression is statistically significance withF value = 96.8 and α<0.01 by using the F test. However, it is important to note that the data are scattered. One possible explanation is that the frequency of light precipitation is high in these regions; the Geonor has large system errors when recording the light precipitation.


## 4. New Method for Calculating the Parsivel Solid Precipitation Amount

By comparing the daily solid precipitation recorded by Parsivel with the corrected Geonor, we found that the Parsivel overestimated the solid precipitation amount in the interior QTP. Normally, the Parsivel can directly measure the number and the falling velocity of particles with different sizes. In this study, we recalculated the precipitation amount by using the size and number of snow particle. The computational formula is as follows:(8)P=π6A∑j=1t∑i=132NiαDi3ρsnowρwater,where P is the solid precipitation amount (mm), t is the precipitation duration (minutes), A is the sampling area (mm2), Di (mm) and Ni are the diameter of particles class i and corresponding particle numbers, α is the snow particles diameter correction factor, and ρsnow (kg/m3) and ρwater (kg/m3) are density of snow and water, respectively. When calculating the SPC solid precipitation, Sugiura et al. [8] set the ρsnow as 917 kg/m3; this value was also used in this study.


### 4.1. Determination of Snow Particles Diameter Correction Factor (α)

To acquire accurate solid precipitation amount from Parsivel, it is necessary to get the equivalent diameter of each snow particle. Compared with the raindrop, the shape of snow grain is more irregular. It is still a challenge to get the equivalent diameter of snow grains. In this study, the particles diameter correction factor (α) was proposed to get the equivalent diameter of snow grains; a statistical approach was used for the calculation of α; the calculation processes were as follows:(1)
Equation (7) was used for correction of Geonor’s half-hour solid precipitation with small wind speed and setting the corrected precipitation amount (Pc-Geonor) as the “true” value.(2)
Choose the corresponding snow particle information and use (8) for calculation. Considering the small particles (D<1 mm) are mainly single grain and the larger particles (D>1 mm) are mainly granular aggregate based on the field observation, the calculation was divided into two parts as follows:(9)π6A∑j=1t∑i=18NiαD<1Di3ρsnowρwater+π6A∑j=1t∑i=932NiαD>1Di3ρsnowρwater=Pc-Geonor,where αD<1 is the snow particles diameter correction factor when D<1 mm and αD>1 is the correction factor when D>1 mm. The meaning of other parameters was the same with (8).(3)
The least square method was used to calculateαD<1 and αD>1.Based on the above method, 81 samples with wind speed smaller than 3 m/s in TGL station were chosen to determineα in the interior QTP, and the results were αD<1=0.72 and αD>1=0.3446.


### 4.2. Recalculation of Monthly and Daily Solid Precipitation in TGL Station

Based on (8), the monthly solid precipitation derived from Parsivel was recalculated. In the WDL station, the routine meteorological data were missing during the study periods; we only compared recalculated Parsivel’s monthly precipitation with Geonor’s corrected precipitation in TGL station; the results were shown in Figure 9. During the study periods, the total precipitation amount recorded by Geonor is 29.4 mm, and Geonor’s total precipitation had increased to 66.5 mm after correction. After recalculation, Parsivel’s total precipitation was 66 mm during this period, which was nearly equal to the corrected Geonor’s. It was important to note that there were still differences between the recalculated Parsivel (Pr-Parsivel) and the corrected Geonor (Pc-Geonor) at monthly scale, especially when the monthly precipitation was small, and the differences were larger. This was also related with Geonor’s bad performance in recording light precipitation.Figure 9
Comparing the monthly recalculated Parsivel solid precipitation with the corrected Geonor precipitation.The recalculated daily solid precipitation of Parsivel(Pr-Parsivel) was also compared with the corrected Geonor (Pc-Geonor) by (7); the results were shown in Figure 10. By using the new calculation method, the Pr-Parsivel value was close to Pc-Geonor based on the method proposed in this study. That means that the new calculation method is suitable for recalculating Parsivel’s solid precipitation in the interior QTP.Figure 10
Comparing the daily recalculated Parsivel solid precipitation with the corrected Geonor precipitation in TGL station.


## 4.1. Determination of Snow Particles Diameter Correction Factor (α)

To acquire accurate solid precipitation amount from Parsivel, it is necessary to get the equivalent diameter of each snow particle. Compared with the raindrop, the shape of snow grain is more irregular. It is still a challenge to get the equivalent diameter of snow grains. In this study, the particles diameter correction factor (α) was proposed to get the equivalent diameter of snow grains; a statistical approach was used for the calculation of α; the calculation processes were as follows:(1)
Equation (7) was used for correction of Geonor’s half-hour solid precipitation with small wind speed and setting the corrected precipitation amount (Pc-Geonor) as the “true” value.(2)
Choose the corresponding snow particle information and use (8) for calculation. Considering the small particles (D<1 mm) are mainly single grain and the larger particles (D>1 mm) are mainly granular aggregate based on the field observation, the calculation was divided into two parts as follows:(9)π6A∑j=1t∑i=18NiαD<1Di3ρsnowρwater+π6A∑j=1t∑i=932NiαD>1Di3ρsnowρwater=Pc-Geonor,where αD<1 is the snow particles diameter correction factor when D<1 mm and αD>1 is the correction factor when D>1 mm. The meaning of other parameters was the same with (8).(3)
The least square method was used to calculateαD<1 and αD>1.Based on the above method, 81 samples with wind speed smaller than 3 m/s in TGL station were chosen to determineα in the interior QTP, and the results were αD<1=0.72 and αD>1=0.3446.


## 4.2. Recalculation of Monthly and Daily Solid Precipitation in TGL Station

Based on (8), the monthly solid precipitation derived from Parsivel was recalculated. In the WDL station, the routine meteorological data were missing during the study periods; we only compared recalculated Parsivel’s monthly precipitation with Geonor’s corrected precipitation in TGL station; the results were shown in Figure 9. During the study periods, the total precipitation amount recorded by Geonor is 29.4 mm, and Geonor’s total precipitation had increased to 66.5 mm after correction. After recalculation, Parsivel’s total precipitation was 66 mm during this period, which was nearly equal to the corrected Geonor’s. It was important to note that there were still differences between the recalculated Parsivel (Pr-Parsivel) and the corrected Geonor (Pc-Geonor) at monthly scale, especially when the monthly precipitation was small, and the differences were larger. This was also related with Geonor’s bad performance in recording light precipitation.Figure 9
Comparing the monthly recalculated Parsivel solid precipitation with the corrected Geonor precipitation.The recalculated daily solid precipitation of Parsivel(Pr-Parsivel) was also compared with the corrected Geonor (Pc-Geonor) by (7); the results were shown in Figure 10. By using the new calculation method, the Pr-Parsivel value was close to Pc-Geonor based on the method proposed in this study. That means that the new calculation method is suitable for recalculating Parsivel’s solid precipitation in the interior QTP.Figure 10
Comparing the daily recalculated Parsivel solid precipitation with the corrected Geonor precipitation in TGL station.


## 5. Discussions and Conclusions

By comparing the solid precipitation amount derived from the Geonor precipitation gauge with LPM and Parsivel in the three meteorological stations in the interior QTP. We came to the conclusions that the Geonor nearly could not catch the light precipitation (the precipitation amount is less than 1 mm during a event) when the wind speed was larger than 3.5 m/s. Even when the wind speed was smaller than 3.5 m/s, about 44% of that light precipitation event still could not be recorded by Geonor. However, the light precipitation is dominant and the wind is strong in winter in the interior QTP. According to our statistics, based on the LPM data in the BLH station, the light precipitation events (the precipitation amount is less than 1 mm during a event) accounted for more than 75% of the total precipitation events in the cold season. So the challenges for getting accurate solid precipitation in the interior QTP are not only correcting the precipitation gauge’s catch efficiency, but also catching the light precipitation in these regions.LPM and Parsivel could detect light solid precipitation that remains and could not detected by Geonor and some other traditional precipitation gauges. By comparing the daily solid precipitation derived from LPM and Parsivel with the corrected Geonor precipitation, we found that LPM can record credible solid precipitation in the interior QTP. However, Parsivel overestimated the precipitation amount. Finally, we concluded that LPM can be effectively conducted in the interior QTP. Taking the LPM’s solid precipitation as the reference value, we also proposed a method for correcting Geonor’s solid precipitation at the hourly scale.In order to get the credible solid precipitation from Parsivel, a new precipitation calculation formula by just using the size and number of snow particles had been proposed in this study, and the diameter correction factor of snow particles was determined by the statistical method. By using the new calculation formula, the accuracy of solid precipitation amount derived form Parsivel had been improved.In summary, the optical instruments have large potential in recording more accurate solid precipitation and they are also powerful tools for recording the high frequency light precipitation in the interior QTP. However, it should be mentioned that both LPM and Parsivel have large errors when used for measuring mixed precipitation. Further efforts need to be made next.



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*Source: 936724-2015-07-27.xml*