Chapter 2 Equations & Numerical Methods

Slides:



Advertisements
Similar presentations
Groundwater Hydraulics Daene C. McKinney
Advertisements

Groundwater Hydraulics Daene C. McKinney
Groundwater Flow Equations
Principles of Groundwater Flow
Yhd Soil and Groundwater Hydrology
Chapter 16 Kruseman and Ridder (1970)
TOPIC 2 STEADY STATE FLOW THROUGH SOIL Course: S0705 – Soil Mechanic Year: 2008.
Conductivity Testing of Unsaturated Soils A Presentation to the Case Western Reserve University May 6, 2004 By Andrew G. Heydinger Department of Civil.
Wedge-shaped and sloping aquifers Adam Forsberg January 28, 2013.
Ground-Water Flow and Solute Transport for the PHAST Simulator Ken Kipp and David Parkhurst.
Continuum Equation and Basic Equation of Water Flow in Soils January 28, 2002.
General governing equation for transient, heterogeneous, and anisotropic conditions Specific Storage S s =  V / (  x  y  z  h)
Subsurface Hydrology Unsaturated Zone Hydrology Groundwater Hydrology (Hydrogeology )
Groundwater 40x larger than lakes+rivers
Analytical and Numerical Solutions are affected by: Differences in conceptual model (confined vs unconfined) Dimensionality (1D vs 2D) Numerical Solutions.
A set of equations that describes the physical and/or chemical processes occurring in a system. Mathematical Model.
Review Of Basic Hydrogeology Principles. Types of Terrestrial Water Groundwater SoilMoisture Surface Water.
Theory of Groundwater Flow
Grad is a vector. q is a vector The dot product of grad and q is div q = 0.
PARTIAL DIFFERENTIAL EQUATIONS
Figure taken from Hornberger et al. (1998). Linear flow paths assumed in Darcy’s law True flow paths.
Figure from Hornberger et al. (1998) Darcy’s data for two different sands.
Conceptual Model A descriptive representation of a groundwater system that incorporates an interpretation of the geological & hydrological conditions.
ESS 454 Hydrogeology Module 3 Principles of Groundwater Flow Point water Head, Validity of Darcy’s Law Diffusion Equation Flow in Unconfined Aquifers &
ESS 454 Hydrogeology Module 2 Properties of Materials Basic Physics Darcy’s Law Characteristics of Aquifers Elasticity and Storage Instructor: Michael.
GROUNDWATER HYDROLOGY II WMA 302 Dr. A.O. Idowu, Dr. J.A. Awomeso and Dr O.Z. Ojekunle Dept of Water Res. Magt. & Agromet UNAAB. Abeokuta. Ogun State Nigeria.
Cross Section of Unconfined and Confined Aquifers
Dr. James M. Martin-Hayden Associate Professor Dr. James M. Martin-Hayden Associate Professor (419)
Theory of Groundwater Flow
Darcy’s Law and Flow CIVE Darcy allows an estimate of: the velocity or flow rate moving within the aquifer the average time of travel from the head.
Aquifer Storage Properties CVEG 5243 Ground Water Hydrology T. Soerens.
Contaminant Transport CIVE 7332 Lecture 3. Transport Processes Advection The process by which solutes are transported by the bulk of motion of the flowing.
Groundwater pumping to remediate groundwater pollution March 5, 2002.
General governing equation for steady-state, heterogeneous, anisotropic conditions 2D Laplace Eqn. --Homogeneous and isotropic aquifer without a sink/source.
Groundwater Jeopardy What is primary porosity? Porosity between grains
CHAPTER SEVEN INTRODUCTORY WELL HYDROLOGY. GROUNDWATER OCCURRENCE.
PRINCIPLES OF GROUNDWATER FLOW. I.Introduction “Groundwater processes energy in several forms”
Lecture 20 Ground Water (3) Ground water movement
Principles of Groundwater Flow
Darcy’s Law Philip B. Bedient Civil and Environmental Engineering Rice University.
CE 3354 Engineering Hydrology Lecture 21: Groundwater Hydrology Concepts – Part 1 1.
How does groundwater flow ? February 26, TOC  Definitions  Groundwater flow overview Equipotentials and flowlines  Wells  Laplace  Boundary.
CE 3354 Engineering Hydrology
Lecture 9.5 & 10 Storage in confined aquifers Specific storage & storage coefficient.
Groundwater Flow Equations Groundwater Hydraulics Daene C. McKinney.
Groundwater Systems D Nagesh Kumar, IISc Water Resources Planning and Management: M8L3 Water Resources System Modeling.
Water Resources Assessment Main Resources – Surface water – Groundwater – Unconventional Tools – Flood routing/delineation models – Runoff models – GIS.
Grad is a vector q = - K grad h Darcy’s law. q is a vector Transient mass balance equation:
Groundwater Review Aquifers and Groundwater Porosity
Flow in Aquifers – 1 Confined Aquifer Flow
CHAPTER III LAPLACE TRANSFORM
Principles of Groundwater Flow
Flow to Wells – 2 Steady flow to a well in an unconfined aquifer
Lecture 20 Ground Water (3) Ground water movement
Algebra.
Aquifers and Groundwater flow
Transient Water Balance Eqn.
Example Estimate the average drawdown over an area where 25 million m3 of water has been pumped through a number of uniformly distributed wells.
Contaminant Transport Equations
Finite Difference Method
Philip B. Bedient Civil and Environmental Engineering Rice University
Transport Modeling in Groundwater
Groundwater hydraulics – lecture 8
Groundwater and well hydraulics
Ground Water Basics continued
Conceptual Model A descriptive representation of a groundwater system that incorporates an interpretation of the geological & hydrological conditions.
APPLICATION OF LINEAR ALGEBRA IN MECHANICAL ENGINEERING
Transport Modeling in Groundwater
Philip B. Bedient Civil and Environmental Engineering Rice University
Solving Systems of Linear Equations by Elimination
Presentation transcript:

Chapter 2 Equations & Numerical Methods

1.1 Governing Equations 1.1.1 Confined Aquifer The governing flow equation for confined aquifers is developed from application of the law of mass conservation (continuity principle) to the elemental volume. Continuity is given by: Rate of mass accumulation = Rate of mass inflow - Rate of mass outflow

Integrating the conservation of mass with Darcy’s Law, the general flow equation in three dimensions for a heterogeneous anisotropic material is derived:

Assuming that the material is homogeneous, i. e Assuming that the material is homogeneous, i.e. K does not vary with position, Equation 2-19 can be written as:

or, combining partial derivatives: If the material is both homogeneous and isotropic, i.e. Kx = Ky = Kz , then Equation 2-21 becomes: or, combining partial derivatives:

Using the definitions for storage coefficient, (S =MSs ), and transmissivity, (T = KM), where M is the aquifer thickness, Equation 2-22 becomes:

Equation 2-24 is known as the Laplace equation. If the flow is steady-state, the hydraulic head does not vary with time and Equation 2-22 becomes: Equation 2-24 is known as the Laplace equation.

1.1.2 Unconfined Aquifer In an unconfined aquifer, the saturated thickness of the aquifer changes with time as the hydraulic head changes. Therefore, the ability of the aquifer to transmit water (the transmissivity) is not constant:

For a homogeneous, isotropic aquifer, the general equation governing unconfined flow is known as the Boussonesq equation and is given by:

If the change in the elevation of the water table is small in comparison to the saturated thickness of the aquifer, the variable thickness h can be replaced with an average thickness b that is assumed to be constant over the aquifer. Equation 2-26 can then be linearized to the form:

1.2 Mathematic Model 1.2.1 Unconfined aquifer

1.2 Mathematic Model 1.2.2 Confined aquifer

1.3.1 FDM: Finite Differences Method 1.3 Numerical Methods 1.3.1 FDM: Finite Differences Method

1.3.2 FEM: Finite Element Method 1.3 Numerical Methods 1.3.2 FEM: Finite Element Method