## Problem

Precipitation estimates over large areas are needed for many purposes, yet precipitation is typically only measured at points in small buckets. How do we estimate the spatial average precipitation for a large area using point measurements?

## Goal

The goal of this exercise is to calculate the total annual depth of precipitation in the DCEW by averaging weighing bucket gauge data from meteorological stations using the hypsometric method, Thiessen polygons, and direct averaging.

## Learning objectives

Upon completion of this exercise, students will be able to:

- Describe the weighted average approach for estimating the average precipitation over a watershed from multiple gauges
- Obtain weight factors using hypsometric, Thiessen polygon, and direct average methods
- Construct Thiessen polygons
- Construct a hypsometric function from a histogram of elevation data
- Develop a mathematical equation expressing the relationship between precipitation and elevation
- Combine a hypsometric function with a precipitation-elevation relationship to produce an elevation weighted average precipitation depth

## Project Files

## Requirements and Connections

- This exercise requires historical hourly precipitation data collected from meteorological stations at varied elevations within DCEW.
- Products of this exercise maybe used by the Watershed Water Balance exercise.

Precipitation is typically measured in tipping or weighing bucket gauges 8-12 inches diameter. Hydrologists, however, are interested in precipitation over a region or watershed. If there were no spatial variability in precipitation, a single bucket in a watershed would be sufficient. This is not the case. Precipitation is highly variable. When multiple gauges area available, the spatial average precipitation must be calculated from point measurements. A weighed average approach is commonly used:where P is the precipitation measured at a gauge (g), G is the total number of gauges, and w is the weight assigned to a gauge. Most common approaches to estimate spatial average of multiple gauges are simply methods to assign weights. For example, we could elect to simply take the direct average of all of our gauges. In this case, each gauge gets an equal weight. If G = 3, each gauge gets a weight of 1/3. This is the same as same as simply adding up each P and dividing by the number of gauges.

A problem with the direct averaging approach is it assumes that the gauges are placed in a way that captures the actual spatial variability. For example, we know that in mountainous terrain precipitation tends to be higher at higher elevations in a watershed. If all of our gauges are placed at high elevations, we will overestimate the average. If the gauges, however, are placed throughout the watershed in a way that appropriately represents the relationship between precipitation and elevation, our direct average will be more accurate. This, however, is not commonly possible. Instead, we can use the hypsometric method. The term hypsometry refers to the measurement of elevation.

The hypsometric method combines the distribution of elevation within a watershed with a know relationship between precipitation and elevation to determine weights for elevation classes. Other commonly used methods to assign weights include Thiessen polygons based on proximity of gauges, and isohyetal methods based on precipitation contours. An advantage of the hypsometric method in mountainous terrain is that is accounts for the mechanism that is known to produce spatial variability of precipitation.

## Hypsometric Method: Developing the Precipitation-Elevation function

The hypsometric method for estimating spatial average precipitation uses a known relationship between precipitation and elevation (Figure 1) with a known distribution of elevations within a watershed (Figure 2). Figure 1 tells us how much precipitation falls at an elevation, or within an elevation zone, and Figure 2 tells us how much of a watershed area is within an elevation zone. In other words, the equation in Figure 1 replaces the gauges and Figure 2 provides the weights.

The precipitation-elevation function is often called the orographic equation after the orographic effect that causes precipitation to increase with elevation. If precipitation gauges are distribution along an elevation range with a watershed, we can obtain a mathematical relationship between the elevation of the gauge and the total precipitation collected by the gauge for a specified time period. Most commonly, the specified time period is one year. It is important to recognize the precipitation-elevation equations can only be applied at time periods for which they were developed. If total annual precipitation was used to develop the equation, the equation cannot be applied to specific storms, seasons, or any other sub-annual time period. Nor should equations from one year be applied to another year, or from one watershed to another watershed. These latter statements are guidelines rather than rules. Although not ideal, it may not be a bad assumption that the precipitation-elevation remains relatively stable from year to year, or that neighboring watershed may be represented by similar functions.

Most certainly, however, a precipitation-elevation function from the foothills near Boise Idaho should not be used to model precipitation in Idaho’s Sawtooth Mountains.After gathering precipitation totals for each gauge, the mathematical equation can be developed. Most commonly, a linear equation of the form below is used:

where P is the precipitation measured at gauge g,

*z*is the elevation of gauge g, and*a*and*b*are curve fitting parameters. The paramater ‘*a*‘ can be considered a precipitation gradient (dP/dz). Once the precipitation-elevation is derived, it replaces the gauges in weighting equation described above. We can calculate the precipitation for any elevation within a watershed, essentially giving us an infinite number of gauges. It is then necessary to determine the distribution of z, called the hypsometric function.## Hypsometric Method: Deriving the Hypsometric Function

Figure 2 presents a hypsometric function for the DCEW. The y-axis spans the range of elevations found in the DCEW. The x-axis gives the proportion of the watershed area that is above any given elevation. The minimum elevation in the watershed plots at 100%, and the maximum elevation plots at 0%. The shape of the curve defines the arrangement of elevations between the minimum and maximum.

Use of the hypsometric function to obtain precipitation gauge weights is typically done by discretizing the continuous function into a histogram of elevation zones (Figure 3). For example, Figure 2 shows that 20% of the watershed is higher than 1700 m elevation and 34% of the watershed is higher than 1600 m elevation. The 1600 m to 1700 m elevation zone therefore occupies 14% of the watershed, as depicted on Figure 3.

Figures 2 and 3 can be derived by analyzing a Digital Elevation Model as described in the Watershed Delineation exercise, or manually by overlaying a regularly spaced grid on an elevation contour map of the watershed (Figure 4).

The number of grid points within an elevation zone divided by the total number of grid points in the watershed is an estimate of the proportion of the watershed in that elevation zone.

## Theisson Polygon Method

In the Thiessen polygon approach, gauges are weighted according their proximity to other gauges. Polygons are drawn around each gauge so that all points within a polygon are closer to the one gauge within the polygon than to any other gauge. Once constructed, the proportion of a polygon relative to the watershed area is used as the gauge weight.

Figures 5 illustrates the steps of the Thiessen Polygon method applied to the Reynolds Creek Experimental Watershed as described in the following steps:

- On a map with the locations of all gauges (Figure 5a), draw lines connecting adjacent gauges (Figure 5b). Draw lightly with a pencil so that your lines can be erased later. Note that is acceptable to use gauges outside of the watershed boundary.
- Draw a perpendicular bisector line at the midpoint of each line from step 1 (Figure 5c).
- From each bisector, draw lines perpendicular to the lines from step 1 until these new lines intersect to form irregular polygons (Figure 5d). This step will take some iteration.
- When polygons look appropriate, eliminate the connecting lines for clarity (Figure 5e).
- Measure the relative area of each subregion. Areas can be obtained using a grid-counting approach as described above.

## Goal

The goal of this project is to calculate the spatial average depth of DCEW annual precipitation using three weighted average approaches including direct average, hypsometric, and Thiessen methods.

The instructions below outline specific steps to follow to complete the calculations. Ensure that you understand the problems and goals of this exercise by reviewing the information in the INTRODUCTION and BACKGROUND tabs.

## Project Files

## Requirements & Connections

- Historical hourly precipitation collected at varied elevations at the following DCEW weather stations: Lower Weather, Treeline, and Bogus Basin (SNOTEL) [zip file]
- Products of this exercise are used by the Watershed Water Balance exercise.

1. Compute the spatial average precipitation by direct averaging

- Download historical 2009 precipitation records and populate the appropriate tabs in the EXCEL workbook provided for:
Note that Lower Weather and Treeline meteorological stations are DCEW stations operated by Boise State. Bogus Basin is operated by the NRCS SNOTEL network. The Bogus Basin site is NOT the same as the Bogus Ridge site, although the two are close to each other. For additional background information about the Bogus Basin site, visit the NRCS.

- Investigate each precipitation record to determine the total depth of precipitation for the year.
- Open the “Tables” tab. For all the meteorological stations, record values from step 1b in the appropriate row in Table 4′.
- Compute the average of all stations in Column E of Table 4.
- Repeat steps 1a-1ed for subsequent years as directed by the instructor.

2. Compute the spatial average precipitation by the hypsometric method

- Develop the precipitation-elevation relationship
- Open the “Tables” tab. Record values from step 1b for all stations in ‘Precipitation (mm)’ column of Table 1.
- View the automatically generated scatter chart of Precipitation (y axis) versus Elevation (x axis). This is only automatic for 1 year; you will need to add new data series for the subsequent years (step 2c).
- Determine the linear relationship between Precipitation and Elevation by adding a linear trendline to the chart. Display the regression coefficient and the equation. Enter the equation parameter values in Table 2.
- Repeat steps 2.a.i through 2.a.iii for other years as directed by the instructor. Populate the designated cells for these years in Table 1 and Table 2 in the ‘Tables” tab of the workbook provided.

- Develop the hypsometric function
- In the “Tables” tab, the ‘Elevation Range’ column in Table 3 contains a list of elevation zones corresponding to those represented in the “Contour Map” tab. Determine the proportion of the watershed in each elevation zone. You can do this manually using a map and grid paper (step a), GIS tools (step b), or a creative way of your choosing (step c):
- Grid paper method:
- Overlay the grid provided on the map (in the “Contour Map” tab), and then count the number of cells or points within each zone [see BACKGROUND]; you can count the number of cells/points directly in Excel or by printing the grid-overlaid-image and counting on paper.
- In the ‘Count’ column enter the number of points or cells that exist within each elevation zone.
- In the ‘Weight (Wg)’ column, use the ‘Count’ data to calculate the proportion of the watershed area that is occupied by each elevation zone.

- GIS method: If you are familiar with geographic information systems such as ArcMap or GRASS you can use a digital elevation model (DEM) to obtain a histogram of elevations classified by elevation zones. Spatial data for Dry Creek are found here: https://earth.boisestate.edu/drycreek/data/spatial-data/
- Method of your choosing: If you use another method to obtain weights, enter your values in the ‘Weight (Wg)’ column and proceed to step 2b.iii.

- Grid paper method:
- In the ‘Cumulative Weight: ∑(Wg)’ column determine the area cumulative weight for each elevation zone; the sum of all weights should equal 1.
- In the ‘Ratio of Area with Higher Z’ column use the “Cumulative Weight: ∑(Wg)” to calculate the elevation band’s ratio of area with higher elevation.
- In the ‘Z’ column enter the mid-point of the elevation zone
- Create a discrete histogram displaying the distribution of elevations within the given elevation bands as illustrated in Figure 3, [see BACKGROUND].
- Create a hypsometric function plot as illustrated in Figure 2, [see BACKGROUND].

- In the “Tables” tab, the ‘Elevation Range’ column in Table 3 contains a list of elevation zones corresponding to those represented in the “Contour Map” tab. Determine the proportion of the watershed in each elevation zone. You can do this manually using a map and grid paper (step a), GIS tools (step b), or a creative way of your choosing (step c):
- Calculate the elevation-weighted precipitation
- In the ‘P(z)’ column, use the linear equation parameter values (Table 2) with the ‘Z’ values (step 2.b.vi) to calculate the precipitation in each zone. It is important the recognize that in this method, the calculated P(z) values replace gauge values in the Equation 1, the precipitation averaging equation described in [see BACKGROUND]. We now have virtual gauges within each elevation zone.
- Calculate the ‘Wg•P(z)’ within each elevation zone.
- Sum the ‘Wg•P(z)’ values to obtain the 2009 total elevation-weighted precipitation.
- Calculate the direct non-weighted average precipitation (across the three meteorological stations) to compare to the results of the hypsometric method.
- Repeat steps 2.c.1 through 2.c.iv for subsequent years, as directed by the instructor, and populate the designated cells in Table 3.
- Record your answers for all analyzed years in ‘Table 4: Summary Table’ in the “Tables” tab of the workbook provided.

3. Compute the spatial average precipitation using the Thiessen Polygon Method

- Open the “Theissen Polygon Workshheet” tab in the Excel workbook for this exercise. You will see the map of Dry Creek including all of the monitoring locations. The orange dots indicate the locations of precipitation gauges. You will construct polygons around each of these orange dots. Note that Bogus Ridge is outside of the watershed boundary. Also note that Bogus Ridge is NOT the same as the Bogus Basin site that you used in the Hypsometric method.
- Follow instructions in the Background section to construct polygons surrounding the following meteorological stations: LW, TL, LDP, SCR, and BR. You can either print the map and construct your polygons with a pencil, or you can export the image to a drawing program and construct the polygons with on a computer. If you use a grid-counting approach to determine polygon areas, record your counts and weights for each polygon in the table provided in the “Thiessen Polygon Worksheet” tab.
- For each precipitation gauge in step 3b, obtain the total precipitation the 2012 water year. You do not have to download the entire dataset as you did for the Hypsometric method. Simply open each file and look for the precipitation value at the end of the year, which is in the last row of the file. Record your values in the table provided in the “Thiessen Polygon Worksheet” tab.
- Using your polygon weights and annual total precipitation values for each gauge, compute the contribution of each polygon to the total precipitation. Sum the precipitation for each polygon to obtain the spatial average precipitation.

The questions below are prompts to think about issues related to hypsometric method, precipitation measurement, and precipitation variability. Consult your instructor to determine if these or other questions are required.- Compare the spatial average precipitation results obtained by the hypsometric, direct average, and if required, thiessen polygon methods. Comment on potential causes for differences.
- How do the parameters of the precipitation-elevation relationship vary from year to year? Is it appropriate to to apply an equation from one year to another year’s data?

Unless instructed otherwise by your instructor, turn in the following:

- Completed ‘Table 4: Summary Table’
- Precipitation-Elevation plots with all years on one plot
- Histogram of elevation distribution
- Hypsometric function plot
- Theissen polygon map
- Answers to discussion questions as directed by instructor
- Evaluation survey for this module.