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Precision and accuracy of streamflow measurements in headwater streams during baseflow

The quantification of baseflow is key for water resources management. However, there are few reports on the precision and accuracy in low streamflow measurements. In this paper, we systematically analyze the precision and accuracy of dilution streamflow measurements in headwater channels during baseflow. Precision refers to the variability of the values for repeated measurements and accuracy is how much the measured value approximates the reference one. We measured streamflow in 31 different cross-sections with contributing areas ranging from 0.02 to 5.33 km2. Streamflow measurements with the current meter were adopted as reference for accuracy estimation. A precision error of ±5.0% was found for the measurements. The percent errors compared to reference streamflow ranged from 0.7 to 45.6%, with a median of 6.1%. Precision and accuracy are in the same order of magnitude found in the literature for larger streams. These results can be used for constraining the uncertainty of streamflow measurements and rainfallrunoff modeling of headwater streams.


INTRODUCTION
Streamflow from headwater is used for drinking water, irrigation, and recreation (Freeman et al., 2007). Headwater streams control a large part of streamflow generation (Sidle et al., 2000) and they remove more nutrients than big streams (Alexander et al., 2000). Most of the time the water that flows in these streams is baseflow, coming from water stored in the soil and rock profiles (Egusa et al., 2016). The baseflow is of ecological importance since some chemical elements important for the biota are better fixed in low flow conditions (Doyle et al., 2005) and it acts as a buffer for changes caused by climate and land use (Van Loon et al., 2012). Therefore, the quantification of the water stored and released as baseflow is key for water resources management (Miller et al., 2016) as well as for the understanding of runoff generation processes in watersheds (e.g. Egusa et al., 2019;. There are three main methods to measure streamflow in natural channels: the velocity-area method; the dilution method; and the use of hydraulic structures such as weirs or flumes (Kondolf & Piégay, 2016). The most common procedure for measuring streamflow is to calculate the average velocity in a crosssection using a current meter along the stream width and depth profile (McMillan et al., 2012). The main types of instruments of the current meter are mechanical (rotations of a propeller) or acoustical (ADCP -acoustic Doppler current profiler). However, it requires a cross-section where the water depth is sufficient for the equipment to work. The use of weirs or flumes requires ad hoc hydraulic works. The dilution method is particularly effective for small streams with irregular channel cross-sections (Bergstrom et al., 2016), its only requirement being that the tracer should be completely mixed with the flow.
Quantifying streamflow measurement errors is crucial as they will be directly translated into uncertainty in hydrologic models (McMillan et al., 2010) and may lead to unnecessary costs due to poor ecological or social decisions (McMillan et al., 2017). Two types of errors in data measurement can be listed: errors related to precision and errors related to accuracy. Precision refers to the variability of the values found for repeated measurements (Day, 1976), which is a measure of "the statistical variance of an estimation procedure" (West, 1999). Accuracy is how much the measured value approximates a reference taken as the correct value (Walther & Moore, 2005).
Streamflow measurement in headwaters is challenging as the channels are usually highly heterogeneous with exposed bedrock, woody debris, cascades, and step-pools (Montgomery & Dietrich, 1989). Even for large-scale rivers, where cross-sections are generally uniform, there is still a lack of information on the expected distributions and magnitudes of error in streamflow observational data (McMillan et al., 2012). Most streamflow measurement errors were estimated for rivers with streamflow in the orders of 10 2 to 10 5 L s -1 (e.g. Benischke & Harum, 1990;Clow & Fleming, 2008;Day, 1976Day, , 1977Kite, 1993), while little is known for headwater rivers on the order of 10 -1 to 10 2 L s -1 (e.g. Bjerve & Grøterud, 1980;Hudson & Fraser, 2002).
In this paper, we systematically analyze the precision and accuracy of streamflow measurements in headwater channels under baseflow conditions. We used field data of first to fourth order catchments with areas ranging from 0.02 to 5.33 km 2 . Measurement errors were estimated using three analyses: (i) the variance of repeated measurements; (ii) the comparison between the streamflow measured using the dilution method and the current meter and; (iii) the errors in relation to the rating curve. In addition, we looked at the relationships between streamflow, drainage area and flow velocity in our data and compared the results with those found in the literature.

Study area
The Peri Lake Watershed is located on Santa Catarina Island, southern Brazil ( Figure 1a). Peri Lake is the largest source of water supply on the island. It is an important ecosystem for biodiversity preservation (Sbroglia & Beltrame, 2012) and in 1981 it was established as a Municipal Conservation Area. The 20 km 2 watershed is surrounded by hillslopes covered with Atlantic rainforest remains and by vegetated sand banks (restinga) that separate the 5.7 km 2 coastal lake from the sea (Figure 1b). It is located in the transition between tropical and temperate climates, the average annual precipitation is 1500 mm, with hot summers and no dry season. The geological formation of the Peri Lake Watershed is granite and dykes in practically its entire structure, with some sedimentary deposits at lower altitudes ( Figure 1c) (Universidade Federal de Santa Catarina, 2018).
Streamflow measurements were made at 31 different crosssections of the Peri Lake Watershed (Figure 1d). There are four main alluvial channel-reach morphologies ( Figure 1e) which were classified according to Montgomery & Buffington (1997). There are 6 alluvial cross-sections in first order streams near the springs. Cascade is the most common channel-reach morphology (22 cross-sections) with drainage areas ranging from 0.13 to 1.13 km 2 in streams of first to third order. Three cross-sections can be classified as steppool. Streams characterized by cascade and step-pool turned into dune ripple near Peri Lake (points 4, 8 and 10 in Figure 1d), they are associated with alluvial deposits (Figure 1c) and low gradient sand channels (Montgomery & Buffington, 1997).

Streamflow measurements
Streamflow was measured using three different methods, depending on the cross-section: the volumetric method, the current meter, and the dilution method. The monitoring occurred on 3/15   (Table 1), during baseflow. We adopted one or more days without rainfall as baseflow conditions. Since the time of concentration of the largest contributing watershed is on the order of 1h (estimated using the formula of Dooge, 1973), we considered that after a day without rainfall there would be only baseflow in the stream.
For the volumetric method we used plastic containers with a volume of 0.25 L and 7 L (Figure 2a). The streamflow was estimated according to the following equation: where Q v is streamflow by the volumetric method [L s -1 ], V is the collected volume [L] and T is the total time of volume collection [s]. The verification that all the water of the cross-section flowed into the container was done visually.
We used a mechanical current meter to estimate streamflow ( Figure 2b). The total streamflow is approximated by measuring the width, depth, and velocity at discrete points along the channel cross-section. The total streamflow in a cross-section is given by: , where x is the horizontal distance of the vertical from the edge of the water (Cohn et al., 2013). To estimate the average velocity at a vertical, velocity was measured at 60% of the height of the vertical, according to the method described in Santos et al. (2001).
According to Hudson & Fraser (2002) there are four assumptions for the slug dilution method: (i) the salt must be completely mixed with the flow at the in-stream measurement point; (ii) the salt must be added to the channel instantaneously; (iii) there must be no local inflows between the injection and measurement points and; (iv) the measured reach should be straight with no pools where the salt can become retarded and separated from the main flow. We used table salt as a tracer for the dilution method. Salt concentration was measured using a conductivity probe (Figure 2c). The streamflow was calculated as: where Q D is the streamflow [L s -1 ] obtained with the dilution method, V is the volume of tracer solution [L], Ct is the concentration of the applied salt solution [g L -1 ], ( ) Cr τ is the concentration of salt in the stream [g L -1 ] at time τ , 0 Cr is the concentration of salt in the stream [g L -1 ] at the time of salt injection, and dτ is the time step (here 5 seconds).
The flow velocity was estimated as: Various strategies were adopted to ensure the complete mixing of the salt in the streams: (i) food coloring was injected into the water and its dilution observed; (ii) in cascade channels the salt injection point and the probe location were at sites where the water flows in a small cross-section and; (iii) in a step-pool channel the salt was injected after the pool.

Precision and accuracy of streamflow measurements
Precision and accuracy analysis of the dilution method was performed for streamflow measurements of each crosssection ( Figure 3). Precision refers to the variability of the values found for repeated measurements (yellow box in Figure 3). The precision can be estimated when there are multiple streamflow measurements (e.g. Day, 1976).
Accuracy is the deviation of a measurement from a reference one. Most of the literature uses the streamflow measured with another method as the reference (or real) value. However, in headwater cross-sections it may not be possible to measure streamflow by more than one method. Therefore, we analyzed the accuracy of the data set in two different ways (grey boxes in Figure 3): (i) in the case that streamflow was measured with more than one method in the same cross-section, the differences between the streamflow measured with salt dilution and the other method were calculated (e.g. Benischke & Harum, 1990;Bjerve & Grøterud, 1980;Davids et al., 2019;Gees, 1990;Kite, 1989); (ii) in cross-section 10 we calculated it as the difference between the streamflow measured with the dilution method and the best fit of the rating curve derived using current meter measurements (e.g. Clow & Fleming, 2008;Hudson & Fraser, 2002).
In addition, we looked at the relationships between streamflow and drainage area, and between specific streamflow and drainage area on various days of measurement and for all our data combined. Lastly, we illustrated the relationship between streamflow and flow velocity we found using the dilution method and the current meter, respectively, and compared our results to data reported in the literature.
The precision is assessed through the percent error about the mean of duplicates and triplicates (Day, 1976). The greater the precision, the lower the error: The accuracy is assessed through the absolute percent error compared to the reference streamflow. The greater the accuracy, the lower the error. In this paper the reference streamflow is either the streamflow measured with the current meter ( CM Q , Equation 6) or the streamflow estimated from the rating curve ( RC Q , Equation 7): where D Q is the streamflow measured using the dilution method [L s -1 ].
The rating curve was derived in cross-section 10 where the water level gauge is located (Ribeirão Grande Watershed, crosssection 10 - Figure 1d). The rating curve was obtained from the best fit of a power-law relationship between streamflow measurements with the current meter and the corresponding water levels: where RC Q is streamflow estimated by the rating curve, H is water level [cm], , á and β are regression constants. Streamflow, flow velocity, and drainage area scaling relationships were assessed. Relating (i.e. scaling) streamflow to the catchment area, which is called "drainage area ratio method", is commonly used to estimate the streamflow in ungauged watersheds (Archfield & Vogel, 2010). Nearby watersheds in the same landscape are often assumed to have similar specific streamflows: where q is specific streamflow [L s -1 km -2 ], Q is streamflow and A is catchment area [km 2 ]. Equation 9 implies that the relationship between streamflow and area is linear. This seems to be the case above an area of around 1 to 2 km 2 (e.g., Archfield & Vogel, 2010;Egusa et al., 2016;Karlsen et al., 2016;Lyon et al., 2012;Woods et al., 1995). In order to verify the variation in the specific streamflow of different monitoring campaigns, we normalized the specific streamflow of each cross-section (qn i ) by dividing the specific streamflow of each cross-section by the specific streamflow of the day (q d ): where qn is the normalized specific streamflow at cross-section i [L s -1 km -2 /L s -1 km -2 ], q is the specific streamflow at cross-section i [L s -1 km -2 ] and d q is the specific streamflow on the day [L s -1 km -2 ]. The specific streamflow for each day was obtained by Equation 9.
According to Leopold & Maddock Junior (1953), the relationship between streamflow and velocity can be described with a power-law (e.g. Bergstrom et al., 2016;Edwardson et al., 2003;Leopold, 1953;Wondzell et al., 2007) where v is the velocity [m h -1 ], a and b are regression constants.

RESULTS
We made a total of 78 streamflow measurements, 12 measurements using the volumetric method (Q V ) ( Table 2), 57 measurements using the dilution method (Q D ) ( Table 3), and 9 measurements using the current meter (Q CM ) ( Table 4). We observed that the volumetric method works well for small colluvial channels (Table 2), while the dilution method is ideal for cascades (Table 3), and a step-pool channel supports the dilution and current method in different cross-sections (Table 3 and Table 4).
With the volumetric method we measured streamflows between 0.01 and 0.29 L s -1 in channels with drainage areas ranging from 0.02 to 0.05 km 2 (Table 2). With the dilution method we measured streamflows between 0.12 and 337.45 L s -1 in channels with drainage areas ranging from 0.02 to 5.33 km 2 (Table 3). Lastly, with the current meter we measured streamflows between 6.0 and 410 L s -1 in channels with drainage areas ranging from 0.26 to 5.33 km 2 ( Table 4).

Precision of streamflow measurements
We assessed the precision using 46 measurements. The percent error about the mean of multiple measurements (error P ) tends to decrease as Q D increases (Figure 4a and b). The first and third quartile of error P of all data were -5.0% and 4.7%, respectively, and the standard deviation was 14.7% (Figure 4b). The largest error P are close to 1 L s -1 .

Accuracy of streamflow measurements
Comparison between dilution (Q D ) and current meter (Q CM ) data In Table 5 the streamflows measured with the dilution method (Q D ) and the current meter (Q CM ) are compared for the seven occasions (cf. Table 4) when both methods were used concurrently. Here we take Q CM as the reference value. In six measurements Q D was lower than Q CM . The percent error compared   Table 4. Description of streamflow measurements with the current meter. 10* is the cross-section downstream, 10** the cross-section immediately upstream, and 10*** the cross-section immediately downstream of the cross-section used to measure streamflow with the dilution method. MD is the Maximum Depth, AD is the Average Depth and DBV is the Distance Between Verticals.  to Q CM (error CM ), which is taken as the reference streamflow here, ranged from 0.70% to 45.63%. The largest error CM was for the lowest streamflow in cross-section 10 ( Figure 1d). Despite the small number of samples, these data are important, given the scarcity of streamflow measurements with more than one method in cross-sections in headwater streams under baseflow conditions.

Comparison between dilution (Q D ) and rating curve (Q RC ) data
In Table 6 the streamflows obtained with the dilution method (Q D ) and the rating curve (Q RC ) are compared for the nine occasions when both methods were used concurrently. Now Q RC Table 6. Difference in streamflow measurement with the dilution method and the rating curve. error RC is the percent error compared to the reference streamflow which is taken here as the one obtained from the rating curve. is taken as the reference value. The absolute percent error ranged from 1.30% to 42.37%, the median was 6.6%. The rating curve ( Figure 5) was derived from measurements with the current meter between March 14, 2017 and September 12, 2018. After that date the cross-section was modified by a severe storm and we could not use the same rating curve.

Streamflow and drainage area
The relationship between streamflow and drainage area can be derived by linear regression (Figure 6). All 55 measurements are fitted quite well by the same regression line (R 2 = 0.68). R 2 was ≥ 0.79 on all individual monitoring days. The measurements made to derive the rating curve were not considered.
Similar qn values are spatially close (Figure 8). In most cases qn values on the east coast (region R1 - Figure 8) are below the 1.00 L s -1 km -2 /L s -1 km -2 in Figure 7. The region R1 (cross-section 2, 4, 6, 7 - Figure 1d) is characterized by a low altitude and the presence of alluvial sediments near the Lake (seen in the field). The drainage area of these cross-sections is < 0.3 km 2 . Cross-sections 8 and 10 are in the same region (Figure 1d), but the drainage area is > 1 km 2 and the qn are close to the 1.00 L s -1 km -2 /L s -1 km -2 .
Cross-section 10 is the outlet of the Ribeirão Grande watershed (Figure 1d). This watershed is characterized by dikes and pasture (Figure 1b, 1c). Cross-section 10 had similar streamflow to cross-section 13 (Figure 1d) on two campaign days. However, the drainage area of cross-section 13 is only half that of cross-section 10. Upstream of cross-section 10, in region R2, cross-sections 12, 13, and 14 have a qn above 1.00 L s -1 km -2 /L s-1 km -2 ( Figure 8).
The data are shown in green in Figure 7 represent crosssections on the same stream in region R3 ( Figure 8) and have qn values close to 1.00 L s -1 km -2 /L s -1 km -2 . The data shown in yellow in Figure 7 are from areas under Atlantic forest and at higher altitudes (region R4 in Figure 8). Here qn is above or near 1.00 L s -1 km -2 /L s -1 km -2 .

Flow velocity and streamflow
We measured the flow velocity 52 times, 43 times with the dilution method (v D ), and 9 times with the current meter (v CM ). There is a power-law relationship (see Equation 11) between v D and Q D (Figure 9 and Table 7) when the entire data set is considered. The regression lines for the current meter data (v CM ) and the data obtained with the dilution method (v D ) have a similar slope (b), but the intercept for the v CM data (a) is about 100 m h -1 lower (Table 7) because the v CM are lower than the v D so that the regression line runs lower (Figure 9). When only cross-sections of first and second order streams are considered, it is not possible to verify a power-law relationship (Table 7).
Our dilution method data lie above or among the data from other studies, while our current meter data lie below them ( Figure 10). We can see in Table 7 that the values of the regression parameters are inside the range found in other studies. All values for a and b in Table 7 have a p-value < 0.05.

Choice of the streamflow measurement method
Here we discuss some particularities observed in the field for each method. All channels where the volumetric method was used are first order and mostly colluvial channels. The main problem related to the use of this method in natural channels is that it is only feasible for small volumes and that all the water of the cross-sections must flow to the same point.
Concerning the slug dilution method, Day (1977) recommends a distance of 25 times the width of the channel so that there is a complete mixing of the tracer in the water. However, the method assumes that the mixing length should be straight with no pools. We noticed that there are pools between Table 7. Values of the parameters a and b in power-law regressions (Equation 11) between streamflow (L s -1 ) and flow velocity (m h -1 ). n is the number of data points in the regression, R 2 reflects the goodness of fit, PLW stands for Peri Lake Watershed.  intervals smaller than 25 times the width of the channel in cascade and step-pool channels, which led us to adopt shorter distances. According to Montgomery & Buffington (1997), step-pool has a pool every 4 times the width of the channel, and cascade has a pool less than 1 time the width of the channel. However, in our study we noticed that this relationship varies with the flow. We observed that the lower the streamflow, the greater the number of pools in the channels. For example, in cross-section 4 ( Figure 1d) the distance between two pools is 6.3 meters with a streamflow of 1.19 L s -1 . When the streamflow was 27.05 L s -1 , the distance between pools increased to 9.7 meters. On June 18, 2020, streamflow was measured in the driest conditions in the watershed encountered during this work. In this campaign the minimum velocity required for the propeller of the current meter to rotate was reached in just 2 of the 14 verticals. Therefore, Q CM was probably below the actual streamflow.

Study
The dilution method was the most appropriate to use in headwater stream because: (i) the irregular channel geometry and turbulent flow conditions ensure the complete mixing of the tracer in the water, while they do not allow the use of the volumetric or current meter method; (ii) streamflow measurements using the dilution method took us on average twenty minutes, while the current meter took us one hour per measurement, and (iii) the equipment used in the dilution method is easier to transport and has a lower cost when compared to the current meter. Also, Davids et al. (2019) concluded that the dilution method yields the most accurate measurements among streamflow measurement methods with low cost and low technical complexity.

Precision and accuracy errors
In our data set streamflow measurements with the dilution method at lower water levels had less spread dispersion around the rating curve than measurements at higher levels ( Figure 5). According to McMillan et al. (2012) the confidence bounds of the rating curve have typical values of 50-100% for low flows, 10-20% for medium or high (in-bank) flows, and a single estimate of 40% for out of bank flows. In our data set there is less uncertainty in the rating curve at lower flow rates, different from what is indicated in the review article of McMillan et al. (2012). Besides, using the dilution method makes it is possible to measure streamflow even at low water levels, where sometimes it is not possible to use a current meter. Because the dilution method showed good results for low streamflow measurements, the use of the dilution method could improve the derivation of the rating curve at low flows. Day (1976) found a percent error about the mean of duplicates and triplicates (error P ) in the dilution method of up to 10 -20%, although such percentages were infrequent. The most probable error P were, however, considerably less, ranging from about 4 to 7%. In Day (1976) streamflow between 130 and 6110 L s -1 was measured, while our streamflow varied between 0.11 and 340 L s -1 . Even with the difference in scale between streamflow, the error P were in the same order of magnitude.
With the current meter, error P may range from 0.3 to 2.8% (Smoot & Carter, 1968), or from 1.4 to 5.1% (Schneider & Smoot, 1976). In the studies of Smoot & Carter (1968) and Schneider & Smoot (1976) the error P is inversely proportional to Q CM , as in our results. Hudson & Fraser (2002) estimated the error RC of streamflow measurements with the dilution method and found it to be 5.5% on average in a stream with a drainage area of 8.6 km 2 . The error RC of our values was on average 9.0% in a stream with a drainage area of 5.3 km 2 . Hence, the values from our study are similar to those of Hudson & Fraser (2002).
In general, the values found in the literature indicate that the error RC (e.g. Clow & Fleming, 2008;Hudson & Fraser, 2002) is smaller than the error when comparing two measurement methods (e.g. Benischke & Harum, 1990;Bjerve & Grøterud, 1980;Davids et al., 2019;Gees, 1990;Kite, 1989). The opposite occurred with the data from our study. When we consider error CM and error RC together the errors are between 3.3 and 19.4% for the first and third percentile.
Other work in the literature found similar measurement errors ( Figure 11), even in rivers with higher streamflow. Figure 11 shows the relative errors as (i) the RMSE of the rating curve (Clow & Fleming, 2008;Hudson & Fraser, 2002); (ii) the average of the percent error compared to a reference streamflow (Benischke & Harum, 1990;Bjerve & Grøterud, 1980;Davids et al., 2019) and; (iii) the most probable percent error compared to reference streamflow (PLW -this study; Gees, 1990;Kite, 1989).

Relationship between streamflow and drainage area
Although there is a high variation in normalized specific streamflow (qn), this variation may not be related to the streamflow measurement errors, but to the characteristics of the watershed. Watersheds with smaller areas have a greater variation in qn than larger watersheds (Figure 7). Our data indicates that the variation of qn tends to decrease once the drainage area exceeds 1 km 2 . Woods et al. (1995) used a current meter to measure streamflow and Figure 11. Variation of absolute percent error compared to reference streamflow from the literature. The squares indicate the average of maximum and minimum percentage error and maximum and minimum streamflow, the whiskers extend to the most extreme data points of streamflow and percent error.

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found that the spatial variability of the baseflow declined markedly when the drainage area reached 0.5 to 2 km 2 . This threshold is called "representative elementary area" (REA).  investigated the REA via the concentration of silica and found a large spatial variation of this concentration until an area of > 0.1 to 1 km 2 was considered. Egusa et al. (2016) found that the REA is around 1 km 2 . The variation in q n may not be related to streamflow measurement errors, because similar REA were determined using different measurement methods.
Some studies show that qn is related to physical characteristics of the watershed, such as altitude (e.g. Egusa et al., 2016;Lyon et al., 2012), vegetation cover (Karlsen et al., 2016;Lyon et al., 2012;Wohl et al., 2012) and exchanges between rivers and the hyporheic zone (e.g. Godsey & Kirchner, 2014). The qn in our study is weakly related to the slope (R 2 = 0.24, data not shown) and the altitude (R 2 = 0.13, data not shown). Cross-sections near the lake have a lower qn, which might be due to water exchanges between the river and the soil, because the soil is formed by alluvial sediment and has a high infiltration capacity. The Peri Lake geology contains dikes, which may explain the exchange of groundwater between sub-basins. In summary, what we observed is that the variation of qn may be associated with: (i) altitude and slope; (ii) water exchanges between the river and the soil; (iii) land cover and; (iv) geological formation.

Relationship between streamflow and flow velocity
The velocity is not uniform across stream networks, because of differences in fluvial geometry (Leopold & Maddock Junior, 1953). The headwater drainage network in our study area is formed mainly by cascade channels where there is a great variation in velocity between cross-sections which change between fast flow and pools. The velocity measured using the dilution method represents an average velocity in the mixing length, while the velocity measured with the current meter represents the velocity of a single crosssection. The choice of the streamflow monitoring cross-section might overestimate the average velocity of the stream when the dilution method is used, since the cross-section is chosen so that there is enough turbulence to ensure complete mixing. On the other hand, the cross-sections chosen to measure streamflow with the current meter must have a sufficient water level to support the operation of the device and this occurs only in cross-sections where the flow is slower. Using the current meter and dilution simultaneously to calculate the velocity is the ideal approach to characterize the flow velocity in the drainage network.
It was not possible to verify a general relationship between velocity and streamflow in first and second order streams under baseflow conditions. One explanation could be that there are two mechanisms that control flow velocity: (i) hydrodynamic dispersion, which occurs within the individual flow channel, and (ii) geomorphological dispersion, which changes according to the geometry of the network (Rinaldo et al., 1991). Both dispersion coefficients increase with increasing stream order (White et al., 2004). If same order streams of a watershed have similar hydraulic patterns, this indicates the velocity must be similar in streams of the same order.

CONCLUSION
We found that the dilution was the best measuring method for the cascade morphology which we found in most of our headwaters. The dilution method is efficient even at low water levels, where the current meter cannot be used. The precision of the dilution measurements was around ±5.0% with a standard deviation of 14.7%. The error compared to a reference streamflow ranged from 0.7 to 45.6%. Precision and accuracy are in the same order of magnitude found in the literature for higher streamflows.
The relationship between streamflow and the drainage area is linear. Watersheds with smaller drainage areas have a greater variation in the specific streamflow between them than larger watersheds. The baseflow of the cross-sections is related to the characteristics of the drainage area and the exchange between the stream and the soil. It was possible to verify the power-law relationship between velocity and streamflow for the data set only when fourth order streams were considered. As can be expected, the first and second order streams are more heterogeneous in geometry and flow velocity. We recommend the use of more than one measurement method in these streams.
Although the accuracy of measured streamflow for first and second order streams has been estimated, knowing the magnitude of absolute errors for these streams is still a challenge. Our results can be applied to improve the quantification of streamflow in headwaters and further constrain the uncertainty estimation in rainfall-runoff modeling. We hope that this work will encourage further research involving streamflow measurements in headwater streams under baseflow conditions.