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         Geoplanning 
     Vol 6, No 2, 2019, 89-98                                                                                                                                                            Journal of Geomatics and Planning 

                                                                                                 E-ISSN: 2355-6544 
http://ejournal.undip.ac.id/index.php/geoplanning 

doi: 10.14710/geoplanning.6.2.89-98  

Modelbuilder and Unit Hydrograph for Flood Prediction and Watershed 
Flow Direction Determination at The West Branch of The Little River, 
Stowe, Lamoille County, Vermont, USA 

F. E. S. Silalahia,b*         , F. Hidayatb   

a Western Michigan University, Geological and Environmental Sciences, USA 
b Geospatial Information Agency, Indonesia 

Abstract: The West Branch of the Little River in Stowe, Lamoille County, Vermont has 
been widely studied, and this area is regularly subject to flooding. The West Branch 
joins the Little River, which flows into the Winooski and drains into Lake Champlain. 
This area has undergone extensive development as an economic response to the ski 
resort industry over the past 50 years, and the recreational pathway is on the banks of 
the river. The Little River is adjusting to the loss of historic floodplain area, channel 
modifications (straightening and gravel mining), and runoff changes. In this project, a 
DEM with 10 and 30 meters resolution will be used to determine the watershed area 
for the outlet point at the south of Stowe for hydrological analysis. This project intends 
to describe the watershed flow direction with a unit hydrograph that shows when 
water discharge at the outlet is at its height during a rainfall event and produce the 
floods prediction map by predicting the nature of flood events to help in planning and 
responding to flood events effectively using ArcGIS Pro 2.0. The results show the time it 
takes water to flow to the outlet ranges from 0 seconds (rain that falls on the outlet 
itself) to over 8 hours and 46 minutes. The amount of water has accumulated, 
indicating that water will flow at its fastest when funneling toward the outlet point 
downstream of the town with no exception, indicating that water will flow at its fastest 
when funneling toward the outlet point downstream of the town. 
 
  

Copyright © 2019 GJGP-UNDIP  
This open access article is distributed under a  

Creative Commons Attribution (CC-BY-NC-SA) 4.0 International license. 

How to cite (APA 6th Style): 
Silalahi, F., & Hidayat, F. (2020). Modelbuilder and Unit Hydrograph for Flood Prediction and Watershed Flow Direction Determination at The West 
Branch of The Little River, Stowe, Lamoille County, Vermont, USA. Geoplanning: Journal of Geomatics and Planning, 6(2), 89-98. doi: 
10.14710/geoplanning.6.2.89-98 

 
 

1. INTRODUCTION 

Hydrological processes are complex (Khan, Yufeng, & Ahmad, 2009). A proportion of the precipitation 
falls on the stream and river network directly and contributes to runoff. The rest of the precipitation 
reaches the ground, which infiltrates through the soils, directly contributing to surface runoff (Guéro, 
2006). Runoff occurring on uplands flows downstream in various patterns affected by spatial and temporal 
distribution of rainfall, rate of snowmelt, hydraulics of streams, watershed and channel storage, geology, 
and soil characteristics, watershed surface and cover conditions (The U.S. Department of Agriculture, 2007). 
Understanding the effect of sediment and changing water input to streamflow is crucial, so it needs to 
know hydraulic resistance by understanding step-pool formations (Sulebakk, 2017; Maxwell & 
Papanicolaou, 2001). 

The West Branch of the Little River in Stowe, Lamoille County, Vermont has been widely studied 
because it is regularly subject to flooding. High flows that would normally access the floodplain are causing 
extensive bank erosion, channel widening, loss of aquatic habitat, and general channel instability (The 
Lamoille County Planning Commission, 2006). A previous study about peak discharges estimation and unit 
hydrographs was developed for streams in Charlotte and Mecklenburg County in 2003. Estimating unit 

Article Info: 
Received: 11 July 2019 
in revised form: 11 September 2019 
Accepted: 11 November 2019 
Available Online: 30 December 2019 
 

Keywords:  
Little River, Flood, Unit Hydrograph, 
Geographic Information Systems 
(GIS), ArcGIS Pro 
 

*Corresponding Author: 
Florence Silalahi 
Western Michigan University, 
Geological and Environmental 
Sciences, USA 
Email: florenceelfriede@gmail.com   

OPEN ACCESS 

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mailto:florenceelfriede@gmail.com


 
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hydrographs is an important component used in watershed modeling and (or) design of stormwater-
management structures. The unit hydrograph includes three statistical relations, i.e., storm peak discharge, 
unit-hydrograph peak discharge, and unit-hydrograph lag time. The statistical relation to estimating the 
storm peak discharge is based on analyses of observed peak discharges regressed against rainfall and basin 
characteristics (Weaver, 2003). 

Flood prediction involves the rainfall-runoff transformation processes based on empirical or combined 
conceptual physically-based descriptions of the processes involved, i.e., rainfall into a flood hydrograph and 
the translation of that hydrograph throughout a watershed or any other hydrologic system (Ramírez, 2000). 
The Unit Hydrograph is the surface runoff hydrograph resulting from one unit of rainfall excess, spatially 
and temporally distributed over a watershed uniformly for a specified duration, which was applied at the 
outlet of the sub-catchment(s) along the river (Guéro, 2006). Despite it categorization as a conservative 
method, the unit hydrograph remains a useful and practical approach to dealing with operational 
hydrological forecasting and rainfall-runoff modelling. Besides, this method can compute the predicted 
time to peak of runoff more accurately for time less than one hour (Kusumastuti & Jokowinarno, 2012). 

In this project, a digital elevation model (DEM) will be used to determine the watershed area for the 
outlet point at the south of Stowe and make it ready for hydrological analysis. It has 10 meters resolution 
and was derived from the United States Geological Survey (USGS). Besides, a pour point feature that 
depicts the outlet downstream of the Little River where a unit hydrograph will be created, a polygon 
boundary that depicts the boundaries of Stowe from Vermont Center for Geographic Information (VCGI), 
and a raster layer with 30 meters resolution that depicts the surface water bodies in the area derived from 
features in the NHDPlus Version 2 dataset are needed. This project intends to describe the watershed flow 
direction with a unit hydrograph that shows when water discharge at the outlet is at its height during a 
rainfall event and predicts flooding that will help plan and respond to flood events effectively. 

 

2. DATA AND METHODS 

As the study area (Figure 1), the West Branch joins the Little River, which flows into the Winooski and 
drains into Lake Champlain. At the Little River's confluence in the Village of Stowe, the elevation is about 
695 feet above sea level. The Mountain Road and the Stowe Recreation Path parallel the West Branch for 
most of its length. Upstream of Ranch Brook, to where the main channel leaves Route 108 (north of Big 
Spring), the channel slope averages approximately 4.5% with a step-pool/cascade-pool morphology.  

 

 

 

Figure 1. Map Location (The Lamoille County Planning Commission, 2006) 

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Land use adjacent to the river is predominately agricultural, commercial, residential, and recreational. 
The valley post-glaciation contained a glacial lake that left well-drained, highly permeable soils up to high 
elevations in the modern valley. The glacial lake(s) also left behind extremely deep silt, sand, and gravel 
(The Lamoille County Planning Commission, 2006). 

This area has undergone extensive development as an economic response to the ski resort industry 
over the past 50 years, and the recreation path is adjacent to most of the river, so the river is adjusting to 
the loss of historic floodplain, channel modifications (straightening and gravel mining), and changes in 
runoff. Between 1995 and 1998, Vermonters suffered nearly $60,000,000 in flood damage. The majority of 
large twentieth-century floods have occurred during the summer (June through August) and are associated 
with intense cloudbursts, which stay in the mountains producing high rainfall amounts. The remainder is 
divided evenly between fall floods and winter/spring floods.  The fall floods (September through 
November) are often associated with hurricanes. In contrast, the winter/spring floods (January through 
April) are associated with rain events, snow events, or snowmelt (The Lamoille County Planning 
Commission, 2006). 

The study will begin with the precondition of the elevation model that requires DEM preparation to 
get accurate hydrological analysis for the area around Stowe. Precondition the elevation model steps, i.e., 
assessing the flow directions, identifying and fulfilling the sinks. 

 

 

Figure 2. Result of Precondition (Sinks Locate as Orange Dot or Area) 
 

The second process is to delineate the watershed. Watershed delineation requires a flow direction of 
the raster layer and an outlet point. The watershed delineating process includes assessing flow direction, 
assessing flow accumulation, and measuring the outlet point's distance. The pour point as an outlet may 
differ slightly due to the DEM's resolution or other inaccuracies. From the stream's actual location, the 
outlet must be precisely located on the stream as rendered in the DEM. So, in measuring the distance to 
the outlet point, the outlet point's location must be mapped to match the stream exactly and get an 
accurate watershed.  

Delineating a watershed requires two components, i.e., a flow direction raster layer and an accurate 
outlet point. A watershed area is an area in which all flowing water will flow toward an outlet point using 
verified-DEM. The watershed represents all areas that flow to the specified outlet (Environmental Systems 
Research Institute, 2018). A watershed is mapped by determining the watershed area upstream of the 
outlet using the watershed tool in ArcGIS Pro. The watershed comprises almost the entirety of Stowe's 
town boundaries. This indicates rather than draining away, almost all rainfall that lands in Stowe will go 
rushing through the actual town. 

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Along with data processing, it is necessary to build geoprocessing workflows. ModelBuilder will be 
used to develop flood hazard models for the study area (see Figure 3). ModelBuilder is a visual 
programming language and it can be exported to Python script (Kraemer & Hale, 2014; Zandbergen, 2015). 
Geoprocessing models help spatial analysis process and documentation of data management automatically. 
ModelBuilder represents a process of geoprocessing tools as diagram chain sequences, using the output of 
one process as the input to another process. ModelBuilder needs geoprocessing tools, map layers, 
datasets, and other data types, and connect all of it into a process by running the model step-by-step, up to 
a selected step, or run the entire model (Armstrong, 2009; Allen, 2011; Kraemer & Hale, 2014; 
Environmental Systems Research Institute, 2018). ModelBuilders obtained from GIS processing can be used 
to predict conditions related to simulation, evaluation, and discovery because it is able to explain the 
solutions to various problems in the spatial context. This model must answer at least six questions, which 
are related to identification of events, locations, trends, optimal paths, patterns, and models, for example 
damage to settlements due to lava flooding (Kumalawati et al., 2013), soil erosion in small forested 
catchment (Csáfordi et al., 2012), an earthquake-induce landslides risk assessment (Zhu, 2010), and flood 
hazard assessment based on basin morphometry (Omran et al., 2011). The ModelBuilder of this research 
was created using ArcGIS Pro 2.0. 

 

 

 

Figure 3. ModelBuilder of Flood Prediction and Watershed Flow Direction Determination at the West 
Branch of the Little River, Vermont, USA 

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The third step is creating a velocity field and isochrones map. The process that needs to be completed 
from the data collection, processing process, and map creations is shown in Figure 2. Creating steps on a 
velocity field, i.e., creating the slope raster, calculating the slope-area term, calculating the velocity field, 
and determining the minimum and maximum velocities limit. 

For the better prediction of flooding events, planes will need to know how long water flow will be and 
when the flow will reach the outlet during a hypothetical rainfall event.  The speed of flowing water must 
be estimated with a velocity field. Construction of a velocity field requires several assumptions, i.e., 1) 
Velocity is spatially variant, which means it affected by slope and flow accumulation; 2) Velocity is uniform 
at a given location at a given time, which means it does not change over time; and 3) Velocity is discharging 
invariant at a given location, which means it does not depend on the location's rate of water 
(Environmental Systems Research Institute, 2018; The U.S. Department of Agriculture, 2007). These 
assumptions will provide a generally accurate velocity field as an approximation of observed phenomena. 

The last step is creating a unit hydrograph. There are five classifications of hydrographs, i.e., natural 
hydrograph, hydrograph unit, dimensionless unit hydrograph, synthetic hydrograph, and dam breach 
hydrograph (Indarto, 2015). In this paper, the unit hydrograph (hydrograph unit) is used in flood prediction, 
which is obtained through the presentation of an isochrone map, which will show the relationship between 
the time and area of water flowing into the outlet.  

The Unit Hydrograph (UH) of a watershed is defined as the direct runoff hydrograph as a result of a 
constant intensity of excess rainfall’s volume that is distributed uniformly over the drainage area for a 
specific duration of effective rainfall. When dealing with a rainfall of different duration, a new unit 
hydrograph must be derived for the new duration. The fundamental assumptions for modeling hydrologic 
systems using unit hydrographs are a) Watersheds respond as linear systems, which implies that the 
proportionality principle that is scaled accordingly; b) The effective rainfall intensity is uniformly distributed 
over the entire river basin; c) The rainfall excess is of constant intensity throughout the rainfall duration; 
and d) The duration of the direct runoff hydrograph (time base) is independent of the effective rainfall 
intensity and depends only on the effective rainfall duration (Ramírez, 2000). The unit volume is usually 
considered to be associated with 1 cm (1 inch) of effective rainfall distributed uniformly over the basin area 
(Environmental Systems Research Institute, 2018; Ramírez, 2000). 

 

 

Figure 4. Flowchart of a Research Process 

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3. RESULT AND DISCUSSION 

Isochrone maps are one way of analyzing a spatiotemporal phenomenon such as accessibility that 
changes through space over time, so in order to determine the number of potential users in a study area, 
we need to know the location of these people through time (van den Berg et al., 2018). For the same 
reason, isochrones need to be mapped to determining how long it takes water to reach the outlet, how fast 
the water flows (velocity), and the extent of the watershed (by calculating the slope and flow accumulation 
area). To determine the watershed, there are two components that are needed, i.e., accurate flow 
direction and outlet point (Environmental Systems Research Institute, 2018). The following equation is used 
to calculate a velocity field: 

V = Vm (sb Ac) / (sb Ac
m) 

Vm is the average velocity of all cells in the watershed, assumed with average value of Vm = 0.1 
(Environmental Systems Research Institute, 2018). The quantity Sb Ac

m is the average slope-area term 
across the watershed, i.e., the number of cells that flow into that cell, or flow accumulation. Each cell in the 
velocity field is assigned a velocity based on the local slope generated from the DEM layer, and the 
upstream contributing area generated from the Stowe fill flow accumulation layer. 

Unit hydrograph analysis refers only to direct runoff and base flow, which is composed of contributions 
from delayed interflow (the portion of the streamflow contributed by infiltrated water that moves laterally 
in the subsurface until it reaches a channel) and groundwater runoff (the flow component contributed to 
the channel by groundwater). Groundwater runoff is extremely slow as compared to surface runoff 
(Ramírez, 2000). In this case UH model structure is assumed to be appropriate to represent catchment 
behavior. 

 

 

Figure 5. Watershed Flow Direction with Unit Hydrograph with 10 meters DEM’s resolution 
 

Total streamflow hydrographs are usually conceptualized as being composed of: a) direct runoff, which 
is composed of contributions from surface runoff (the main contributor to the peak discharge, includes all 
overland flow as well as all precipitation falling directly to the stream channels) and quick interflow (slower 

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than surface runoff, includes quick interflow that contributes to direct runoff, and delayed interflow, which 
contributes to base flow) (Ramírez, 2000). 

The cell values in a flow direction raster layer can normally be one of only eight integers (see Figure 6) : 
1, 2, 4, 8, 16, 32, 64, and 128, which corresponds to the eight possible flow directions (Environmental 
Systems Research Institute, 2018). Figure 5 shows Stowe watershed flow direction is to estimate for each 
cell, the adjacent cell into which water would flow, i.e., 1 and 2 towards the east and southeast. Water that 
falls in the western mountains takes longer than water that falls on the low-lying stream beds closest to the 
outlet. 

 

 

Figure 6. Flow Direction Coding 
 

Flow time is calculated as the length that water must flow divided by the velocity at which it flows (the 
first equation). There are two variables to determine flow length, i.e., flow direction layer and weight layer 
(the third equation), which is represent an impedance, example water flowing through forested land takes 
longer than water flowing over smooth rock because it's impeded by terrain). An equation to calculate flow 
time (Environmental Systems Research Institute, 2018): 

Flow time [T] = Flow Length [L] / Velocity [LT-1] ………   (1) 

Flow time [T] = Flow Length [L] * Weight [L-1T] ……….   (2) 

By combining these equations: 

Weight [L-1T] = 1 / Velocity [LT-1] ……….  (3) 

       

   

Figure 7. Stowe_slope_areaterm and Stowe_time which has been Processed 
 

The Stowe_time layer shows the time it takes water to flow to the outlet ranges from 0 seconds (rain 
that falls on the outlet itself) to about 31612 seconds or ± 8 hours and 46 minutes. The last map as an 
output of this project is an isochrones map (Figure 9) shows contour lines of locations where the water flow 
exhibits equal travel time to the outlet of the watershed. This time interval should be appropriate for the 
Stowe watershed with a time interval of 1800 seconds for every cell per isochrone zone (Environmental 
Systems Research Institute, 2018). These time intervals as the ordinate of the unit hydrograph. 

A DEM with a resolution of 30 meters is also used for additional analysis. The results of DEM processing 
with a resolution of 30 meters also show relatively the same time and water flow trends. However, it can 
be seen in Figure 8 that the Hydrograph unit has a better curve because the DEM 10 meter resolution more 
accurately displays fluctuating differences (discharge of outlets). The Stowe_time layer shows the time it 
takes water to flow to the outlet ranges from 0 seconds (rain that falls on the outlet itself) to about 48,600 
seconds or ± 13 hours 30 minutes. The three hours different have a big impact on rescue time when the 
hazard happens. 

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Based on the amount of water has accumulated, the area around Stowe is no exception, indicating that 
water will flow at its fastest when funneling toward the outlet point downstream of the town. 

 

 

Figure 8. Watershed Flow Direction with Unit Hydrograph with 30 meters DEM’s resolution 
  

 

Figure 9. Flood prediction of The West Branch of Little River, Stowe with 10 meters DEM’s resolution 
 

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4. CONCLUSION 

This paper shows contour lines of locations where the water flow exhibits equal travel time to the outlet 
of the watershed, which is an adjacent cell into integer 1 and 2 towards east and southeast that falls on the 
low-lying stream beds closest to the outlet. The water that falls in the northeast of the study area takes the 
most prolonged (in time) than the other direction because the water flowing through forested land takes 
longer than water flowing over a smooth rock because the plants impede it. From data processing,  

The Stowe_time layer shows the time it takes water to flow to the outlet ranges from 0 seconds (rain 
that falls on the outlet itself) to about 31612 seconds or ± 8 hours and 46 minutes, using DEM with 10 
meters resolution, and about 48,600 seconds or ± 13 hours 30 minutes, using DEM with 30 meters 
resolution. Both of them show the same unit hydrograph and the trend for water flow relatively. But, the 
three hours different have a big impact on rescue time when the hazard happens. Based on the amount of 
water has accumulated, the area around Stowe is no exception, indicating that water will flow at its fastest 
when funneling toward the outlet point downstream of the town. 

 

5. ACKNOWLEDGMENTS 

The writers would like to thank ESRI, USGS, Vermont Center for Geographic Information (VCGI), and The 
Lamoille County Planning Commission, who provided data, related document, tutorial, insight, and expert 
input that greatly assisted the research, although they may not agree with all of the 
interpretations/conclusions of this paper. The writers would like to thank Dr. Peter J. Voice as an advisor for 
this research. The writers also thank the Ministry of Research, Technology, and Higher Education of 
Indonesia through the RISET-PRO scholarship 2017 (Nr. 264/RISET-Pro/FGS/VIII/2017). 

 

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