ype HOBO Weather Station. Measures: rain, wind, gust speed, wind direction, temperature, relative humidity, solar radiation.@en

Explanation of the calibration procedure of the DTS derived temperatures in the Maisbich river, Luxembourg. Note that it only corrects offsets orriginating from the DTS device (Halo, Sensornet, UK). It does NOT correct for periods when the cable is not properly submerged in the stream. The DTS obtained temperatures were calibrated with five independent temperature loggers (TidbiT v2 Temp logger, HOBO, USA) located along the cable at 26, 395, 931, 1111 and 1270 m from the DTS desktop computer, respectively. Note that the investigated branch lies between 717 (V-notch weir Q3) and 1282 m (V-notch weir Q4) from the desktop computer. For each Tidbit temperature logger, which measured at a 6 min interval, a linear relation was determined between the DTS derived temperature and the difference between the TidbiT and DTS derived temperature for the period 4-Apr-2008 until 4-Dec-2008 (dT = a*T_DTS + b). For each Tidbit location a slope (a) and an offset (b) was determined: Tidbit Distance(m) a b T coolbox 26 -1.31 0,0974 T road 395 -0.49 0,0664 T Mai171u 931 -0.69 0,122 T Mai11u 1111 -0.25 0,109 T Q4-2 1270 -0.056 0,0965 Then a lineair relation between distance from the DTS desktop computer and slope (a_slope + b_slope*X), and between distance from desktop computer and offset (a_offset + b_offset*X) was derived, resulting in an offset as a function of distance and DTS derived temperatures. Subsequently, this offset was added to the initial DTS derived temperatures. Tcal = T_DTS + ( a_slope + b_slope*X)T_DTS + (a_offset + b_offset*X) with: a_slope :0.085 b_slope :1.78e-005 a_offset:-1.16 b_offset:8.03e-004 In the last step the distance was reversed, with the upstream V-notch weir Q4 at 0 m. Only the part between V-notch weirs Q4 and Q3 (at 565 m) are shown.@en

Headwater catchments are important contributors to streamflow. They are small, but all combined they influence river flow significantly. To be able to make proper runoff predictions under different climate conditions and changing land use, it is important to have detailed understanding of the discharge processes in the headwater catchments. In this rersearch the possibilities of fibre optic Distributed Temperature Sensing (DTS) are explored to obtain more insight in temporal and spatial discharge dynamics during stormflow. DTS is a technique capable of measuring temperature with high spatial and temporal resolution. The technique relies on short laser pulses that are sent through a fibre optic cable. Throughout the fibre optic cable small parts of the pulses are reflected by disturbances in the glass fibre, of which the exact position is obtained by measuring the travel time of the reflected light. All experiments were done in the Maisbich: a 565 m long, first order stream in Central Luxembourg.@en

Type: Pressure Sensor Keller DCX-4.0, SN 1467 This instrument is based on differential pressure measurement of two absolute sensors. The sensors measure pressure and temperature. Height of V-notch above sensor: -0.0015m. Datasets with correction contain the corrected discharge observed at the Vnotch. The discharge is calculated as Q=Cd*h^2.5 After correcting the logger measurements with hand measured depths we interpolated the difference (dH) Then we determined the factor Cd with discharge measurements which we also interpolated The timing of hand measurements can be corrected to better represent the logged values The last corrections (variable "clean_corr") were made for blocking of the V-notch weir as folows: z1 represents the last good discharge value after which sedimentation slowly starts blocking the weir z2 represents the moment when the blocking is max z3 represents the moment just before cleaning of the weir z4 represents the moment after cleaning of the weir The max difference in discharge is Q(z3)-Q(z4)@en

Type: Van Essen TD-Driver, SN 19613 This instrument measures pressure with one absolute sensor. It also measures temperature. Height V-notch above sensor: 0.0018m. Datasets with correction contain the corrected discharge observed at the Vnotch. The discharge is calculated as Q=Cd*h^2.5 After correcting the logger measurements with hand measured depths we interpolated the difference (dH) Then we determined the factor Cd with discharge measurements which we also interpolated The timing of hand measurements can be corrected to better represent the logged values The last corrections (variable "clean_corr") were made for blocking of the V-notch weir as folows: z1 represents the last good discharge value after which sedimentation slowly starts blocking the weir z2 represents the moment when the blocking is max z3 represents the moment just before cleaning of the weir z4 represents the moment after cleaning of the weir The max difference in discharge is Q(z3)-Q(z4)@en