BASIC HYDRAULIC PRINCIPLES of OPEN-CHANNEL FLOW by Harvey E
Total Page:16
File Type:pdf, Size:1020Kb
Load more
Recommended publications
-
Biological Impacts of the Elwha River Dams and Potential Salmonid Responses to Dam Removal
George R. Pess1, NOAA Fisheries, Northwest Fisheries Science Center, 2725 Montlake Boulevard East, Seattle, Washington 98112 Michael L. McHenry, Lower Elwha Klallam Tribe, 2851 Lower Elwha Road, Port Angeles, Washington 98363 Timothy J. Beechie, and Jeremy Davies, NOAA Fisheries, Northwest Fisheries Science Center, 2725 Montlake Boulevard East, Seattle, Washington 98112 Biological Impacts of the Elwha River Dams and Potential Salmonid Responses to Dam Removal Abstract The Elwha River dams have disconnected the upper and lower Elwha watershed for over 94 years. This has disrupted salmon migration and reduced salmon habitat by 90%. Several historical salmonid populations have been extirpated, and remaining popu- lations are dramatically smaller than estimated historical population size. Dam removal will reconnect upstream habitats which will increase salmonid carrying capacity, and allow the downstream movement of sediment and wood leading to long-term aquatic habitat improvements. We hypothesize that salmonids will respond to the dam removal by establishing persistent, self-sustaining populations above the dams within one to two generations. We collected data on the impacts of the Elwha River dams on salmonid populations and developed predictions of species-specific response dam removal. Coho (Oncorhynchus kisutch), Chinook (O. tshawytscha), and steelhead (O. mykiss) will exhibit the greatest spatial extent due to their initial population size, timing, ability to maneuver past natural barriers, and propensity to utilize the reopened alluvial valleys. Populations of pink (O. gorbuscha), chum (O. keta), and sockeye (O. nerka) salmon will follow in extent and timing because of smaller extant populations below the dams. The initially high sediment loads will increase stray rates from the Elwha and cause deleterious effects in the egg to outmigrant fry stage for all species. -
Hydrogeology
Hydrogeology Principles of Groundwater Flow Lecture 3 1 Hydrostatic pressure The total force acting at the bottom of the prism with area A is Dividing both sides by the area, A ,of the prism 1 2 Hydrostatic Pressure Top of the atmosphere Thus a positive suction corresponds to a negative gage pressure. The dimensions of pressure are F/L2, that is Newton per square meter or pascal (Pa), kiloNewton per square meter or kilopascal (kPa) in SI units Point A is in the saturated zone and the gage pressure is positive. Point B is in the unsaturated zone and the gage pressure is negative. This negative pressure is referred to as a suction or tension. 3 Hydraulic Head The law of hydrostatics states that pressure p can be expressed in terms of height of liquid h measured from the water table (assuming that groundwater is at rest or moving horizontally). This height is called the pressure head: For point A the quantity h is positive whereas it is negative for point B. h = Pf /ϒf = Pf /ρg If the medium is saturated, pore pressure, p, can be measured by the pressure head, h = pf /γf in a piezometer, a nonflowing well. The difference between the altitude of the well, H, and the depth to the water inside the well is the total head, h , at the well. i 2 4 Energy in Groundwater • Groundwater possess mechanical energy in the form of kinetic energy, gravitational potential energy and energy of fluid pressure. • Because the amount of energy vary from place-to-place, groundwater is forced to move from one region to another in order to neutralize the energy differences. -
Geomorphic Classification of Rivers
9.36 Geomorphic Classification of Rivers JM Buffington, U.S. Forest Service, Boise, ID, USA DR Montgomery, University of Washington, Seattle, WA, USA Published by Elsevier Inc. 9.36.1 Introduction 730 9.36.2 Purpose of Classification 730 9.36.3 Types of Channel Classification 731 9.36.3.1 Stream Order 731 9.36.3.2 Process Domains 732 9.36.3.3 Channel Pattern 732 9.36.3.4 Channel–Floodplain Interactions 735 9.36.3.5 Bed Material and Mobility 737 9.36.3.6 Channel Units 739 9.36.3.7 Hierarchical Classifications 739 9.36.3.8 Statistical Classifications 745 9.36.4 Use and Compatibility of Channel Classifications 745 9.36.5 The Rise and Fall of Classifications: Why Are Some Channel Classifications More Used Than Others? 747 9.36.6 Future Needs and Directions 753 9.36.6.1 Standardization and Sample Size 753 9.36.6.2 Remote Sensing 754 9.36.7 Conclusion 755 Acknowledgements 756 References 756 Appendix 762 9.36.1 Introduction 9.36.2 Purpose of Classification Over the last several decades, environmental legislation and a A basic tenet in geomorphology is that ‘form implies process.’As growing awareness of historical human disturbance to rivers such, numerous geomorphic classifications have been de- worldwide (Schumm, 1977; Collins et al., 2003; Surian and veloped for landscapes (Davis, 1899), hillslopes (Varnes, 1958), Rinaldi, 2003; Nilsson et al., 2005; Chin, 2006; Walter and and rivers (Section 9.36.3). The form–process paradigm is a Merritts, 2008) have fostered unprecedented collaboration potentially powerful tool for conducting quantitative geo- among scientists, land managers, and stakeholders to better morphic investigations. -
Calculate the Friction Factor for a Pipe Using the Colebrook-White Equation
TOPIC T2: FLOW IN PIPES AND CHANNELS AUTUMN 2013 Objectives (1) Calculate the friction factor for a pipe using the Colebrook-White equation. (2) Undertake head loss, discharge and sizing calculations for single pipelines. (3) Use head-loss vs discharge relationships to calculate flow in pipe networks. (4) Relate normal depth to discharge for uniform flow in open channels. 1. Pipe flow 1.1 Introduction 1.2 Governing equations for circular pipes 1.3 Laminar pipe flow 1.4 Turbulent pipe flow 1.5 Expressions for the Darcy friction factor, λ 1.6 Other losses 1.7 Pipeline calculations 1.8 Energy and hydraulic grade lines 1.9 Simple pipe networks 1.10 Complex pipe networks (optional) 2. Open-channel flow 2.1 Normal flow 2.2 Hydraulic radius and the drag law 2.3 Friction laws – Chézy and Manning’s formulae 2.4 Open-channel flow calculations 2.5 Conveyance 2.6 Optimal shape of cross-section Appendix References Chadwick and Morfett (2013) – Chapters 4, 5 Hamill (2011) – Chapters 6, 8 White (2011) – Chapters 6, 10 (note: uses f = 4cf = λ for “friction factor”) Massey (2011) – Chapters 6, 7 (note: uses f = cf = λ/4 for “friction factor”) Hydraulics 2 T2-1 David Apsley 1. PIPE FLOW 1.1 Introduction The flow of water, oil, air and gas in pipes is of great importance to engineers. In particular, the design of distribution systems depends on the relationship between discharge (Q), diameter (D) and available head (h). Flow Regimes: Laminar or Turbulent laminar In 1883, Osborne Reynolds demonstrated the occurrence of two regimes of flow – laminar or turbulent – according to the size of a dimensionless parameter later named the Reynolds number. -
Intermittency As a Transition to Turbulence in Pipes: a Long Tradition from Reynolds to the 21St Century Christophe Letellier
Intermittency as a transition to turbulence in pipes: A long tradition from Reynolds to the 21st century Christophe Letellier To cite this version: Christophe Letellier. Intermittency as a transition to turbulence in pipes: A long tradition from Reynolds to the 21st century. Comptes Rendus Mécanique, Elsevier Masson, 2017, 345 (9), pp.642- 659. 10.1016/j.crme.2017.06.004. hal-02130924 HAL Id: hal-02130924 https://hal.archives-ouvertes.fr/hal-02130924 Submitted on 16 May 2019 HAL is a multi-disciplinary open access L’archive ouverte pluridisciplinaire HAL, est archive for the deposit and dissemination of sci- destinée au dépôt et à la diffusion de documents entific research documents, whether they are pub- scientifiques de niveau recherche, publiés ou non, lished or not. The documents may come from émanant des établissements d’enseignement et de teaching and research institutions in France or recherche français ou étrangers, des laboratoires abroad, or from public or private research centers. publics ou privés. Distributed under a Creative Commons Attribution - NonCommercial - NoDerivatives| 4.0 International License C. R. Mecanique 345 (2017) 642–659 Contents lists available at ScienceDirect Comptes Rendus Mecanique www.sciencedirect.com A century of fluid mechanics: 1870–1970 / Un siècle de mécanique des fluides : 1870–1970 Intermittency as a transition to turbulence in pipes: A long tradition from Reynolds to the 21st century Les intermittencies comme transition vers la turbulence dans des tuyaux : Une longue tradition, de Reynolds au XXIe siècle Christophe Letellier Normandie Université, CORIA, avenue de l’Université, 76800 Saint-Étienne-du-Rouvray, France a r t i c l e i n f o a b s t r a c t Article history: Intermittencies are commonly observed in fluid mechanics, and particularly, in pipe Received 21 October 2016 flows. -
CPT-Geoenviron-Guide-2Nd-Edition
Engineering Units Multiples Micro (P) = 10-6 Milli (m) = 10-3 Kilo (k) = 10+3 Mega (M) = 10+6 Imperial Units SI Units Length feet (ft) meter (m) Area square feet (ft2) square meter (m2) Force pounds (p) Newton (N) Pressure/Stress pounds/foot2 (psf) Pascal (Pa) = (N/m2) Multiple Units Length inches (in) millimeter (mm) Area square feet (ft2) square millimeter (mm2) Force ton (t) kilonewton (kN) Pressure/Stress pounds/inch2 (psi) kilonewton/meter2 kPa) tons/foot2 (tsf) meganewton/meter2 (MPa) Conversion Factors Force: 1 ton = 9.8 kN 1 kg = 9.8 N Pressure/Stress 1kg/cm2 = 100 kPa = 100 kN/m2 = 1 bar 1 tsf = 96 kPa (~100 kPa = 0.1 MPa) 1 t/m2 ~ 10 kPa 14.5 psi = 100 kPa 2.31 foot of water = 1 psi 1 meter of water = 10 kPa Derived Values from CPT Friction ratio: Rf = (fs/qt) x 100% Corrected cone resistance: qt = qc + u2(1-a) Net cone resistance: qn = qt – Vvo Excess pore pressure: 'u = u2 – u0 Pore pressure ratio: Bq = 'u / qn Normalized excess pore pressure: U = (ut – u0) / (ui – u0) where: ut is the pore pressure at time t in a dissipation test, and ui is the initial pore pressure at the start of the dissipation test Guide to Cone Penetration Testing for Geo-Environmental Engineering By P. K. Robertson and K.L. Cabal (Robertson) Gregg Drilling & Testing, Inc. 2nd Edition December 2008 Gregg Drilling & Testing, Inc. Corporate Headquarters 2726 Walnut Avenue Signal Hill, California 90755 Telephone: (562) 427-6899 Fax: (562) 427-3314 E-mail: [email protected] Website: www.greggdrilling.com The publisher and the author make no warranties or representations of any kind concerning the accuracy or suitability of the information contained in this guide for any purpose and cannot accept any legal responsibility for any errors or omissions that may have been made. -
Logistic Analysis of Channel Pattern Thresholds: Meandering, Braiding, and Incising
Geomorphology 38Ž. 2001 281–300 www.elsevier.nlrlocatergeomorph Logistic analysis of channel pattern thresholds: meandering, braiding, and incising Brian P. Bledsoe), Chester C. Watson 1 Department of CiÕil Engineering, Colorado State UniÕersity, Fort Collins, CO 80523, USA Received 22 April 2000; received in revised form 10 October 2000; accepted 8 November 2000 Abstract A large and geographically diverse data set consisting of meandering, braiding, incising, and post-incision equilibrium streams was used in conjunction with logistic regression analysis to develop a probabilistic approach to predicting thresholds of channel pattern and instability. An energy-based index was developed for estimating the risk of channel instability associated with specific stream power relative to sedimentary characteristics. The strong significance of the 74 statistical models examined suggests that logistic regression analysis is an appropriate and effective technique for associating basic hydraulic data with various channel forms. The probabilistic diagrams resulting from these analyses depict a more realistic assessment of the uncertainty associated with previously identified thresholds of channel form and instability and provide a means of gauging channel sensitivity to changes in controlling variables. q 2001 Elsevier Science B.V. All rights reserved. Keywords: Channel stability; Braiding; Incision; Stream power; Logistic regression 1. Introduction loads, loss of riparian habitat because of stream bank erosion, and changes in the predictability and vari- Excess stream power may result in a transition ability of flow and sediment transport characteristics from a meandering channel to a braiding or incising relative to aquatic life cyclesŽ. Waters, 1995 . In channel that is characteristically unstableŽ Schumm, addition, braiding and incising channels frequently 1977; Werritty, 1997. -
Basic Principles of Flow of Liquid and Particles in a Pipeline
1. BASIC PRINCIPLES OF FLOW OF LIQUID AND PARTICLES IN A PIPELINE 1.1 LIQUID FLOW The principles of the flow of a substance in a pressurised pipeline are governed by the basic physical laws of conservation of mass, momentum and energy. The conservation laws are expressed mathematically by means of balance equations. In the most general case, these are the differential equations, which describe the flow process in general conditions in an infinitesimal control volume. Simpler equations may be obtained by implementing the specific flow conditions characteristic of a chosen control volume. 1.1.1 Conservation of mass Conservation of mass in a control volume (CV) is written in the form: the rate of mass input = the rate of mass output + the rate of mass accumulation. Thus d ()mass =−()qq dt ∑ outlet inlet in which q [kg/s] is the total mass flow rate through all boundaries of the CV. In the general case of unsteady flow of a compressible substance of density ρ, the differential equation evaluating mass balance (or continuity) is ∂ρ G G +∇.()ρV =0 (1.1) ∂t G in which t denotes time and V velocity vector. For incompressible (ρ = const.) liquid and steady (∂ρ/∂t = 0) flow the equation is given in its simplest form ∂vx ∂vy ∂vz ++=0 (1.2). ∂x ∂y ∂z The physical explanation of the equation is that the mass flow rates qm = ρVA [kg/s] for steady flow at the inlet and outlet of the control volume are equal. Expressed in terms of the mean values of quantities at the inlet and outlet of the control volume, given by a pipeline length section, the equation is 1.1 1.2 CHAPTER 1 qm = ρVA = const. -
Table of Common Symbols Used in Hydrogeology
Common Symbols used in GEOL 473/573 A Area [L2] b Saturated thickness of an aquifer [L] d Diameter [L] e void ratio (dimensionless) or e1 is a constant = 2.718281828... f Number of head drops in a flow of net F Force [M L T-2 ] g Acceleration due to gravity [9.81 m/s2] h Hydraulic head [L] (Total hydraulic head; h = ψ + z) ho Initial hydraulic head [L], generally an initial condition or a boundary condition dh/dL Hydraulic gradient [dimensionless] sometimes expressed as i 2 ki Intrinsic permeability [L ] K Hydraulic conductivity [L T-1] -1 Kx, Ky , Kz Hydraulic conductivity in the x, y, or z direction [L T ] L Length from one point to another [L] n Porosity [dimensionless] ne Effective porosity [dimensionless] q Specific discharge [L T-1] (Darcy flux or Darcy velocity) -1 qx, qy, qz Specific discharge in the x, y, or z direction [L T ] Q Flow rate [L3 T-1] (discharge) p Number of stream tubes in a flow of net P Pressure [M L-1T-2] r Radial coordinate [L] rw Radius of well over screened interval [L] Re Reynolds’ number [dimensionless] s Drawdown in an aquifer [L] S Storativity [dimensionless] (Coefficient of storage) -1 Ss Specific storage [L ] Sy Specific yield [dimensionless] t Time [T] T Transmissivity [L2 T-1] or Temperature (degrees) u Theis’ number [dimensionless} or used for fluid pressure (P) in engineering v Pore-water velocity [L T-1] (Average linear velocity) V Volume [L3] 3 VT Total volume of a soil core [L ] 3 Vv Volume voids in a soil core [L ] 3 Vw Volume of water in the voids of a soil core [L ] Vs Volume soilds in a soil -
Relationships Among Basin Area, Sediment Transport Mechanisms and Wood Storage in Mountain Basins of the Dolomites (Italian Alps)
Monitoring, Simulation, Prevention and Remediation of Dense Debris Flows II 163 Relationships among basin area, sediment transport mechanisms and wood storage in mountain basins of the Dolomites (Italian Alps) E. Rigon, F. Comiti, L. Mao & M. A. Lenzi Department of Land and Agro-Forest Environments, University of Padova, Legnaro, Padova, Italy Abstract The present work analyses the linkages between basin geology, shallow landslides, streambed morphology and debris flow occurrence in several small watersheds of the Dolomites (Italian Alps). Field survey and GIS analysis were carried out in order to seek correlations among basin area, basin geology, spatial frequency of landslides, in-channel wood storage, and local bed slope. Keywords: large woody debris, landslides, bed morphology, Alps. 1 Introduction Along with sediments, shallow landslides in forested basins supply channels with wood elements, which may have a strong impact on both channel morphology/stability and on debris flow dynamics. Headwater channels, which make up 60–80% of the cumulative channel length in mountainous terrain [10, 11], are characterized by a strong coupling between hillslope and channel processes, in contrast to lowland streams. The switch between different transport mechanisms (e.g., bedload transport to debris flows) in the same channel often depends on the occurrence of shallow landslides feeding sediment in otherwise sediment-limited systems. Along with sediments, shallow landslides in forested basins supply channels with wood elements, which may have a strong impact on both channel morphology/stability WIT Transactions on Engineering Sciences, Vol 60, © 2008 WIT Press www.witpress.com, ISSN 1743-3533 (on-line) doi:10.2495/DEB080171 164 Monitoring, Simulation, Prevention and Remediation of Dense Debris Flows II and on debris flow dynamics. -
Horizons River and Channel Morphology Report Version3
River and channel morphology: Technical Report prepared for Horizons Regional Council Measuring and monitoring channel morphology Dr. Ian Fuller Geography Programme School of People, Environment & Planning March 2007 River and channel morphology: Technical Report prepared for Horizons Regional Council Measuring and monitoring channel morphology Author: Dr. Ian Fuller Geography Programme School of People, Environment & Planning Reviewed By: Graeme Smart Fluvial Scientist NIWA Cover Photo: Tapuaeroa River, East Cape March 2007 Report 2007/EXT/773 FOREWORD As part of a review of the Fluvial Research Programme, Horizons Regional Council have engaged experts in the field of fluvial geomorphology to produce a report answering several key questions related to channel morphology and linkages with instream habitat diversity in Rivers of the Manawatu-Wanganui Region. This report is aimed at introducing concepts of the importance of morphological diversity in the Region’s rivers to the planning framework (to be used in the development of Horizons second generation Regional Plan – the One Plan). This expert advice has been used in the development of permitted activity baselines for activities in the beds of rivers and lakes which may influence the channel morphology and to address the cumulative impacts of these activities over time and space. Monitoring recommendations within this report provide guidance for the management of cumulative reductions in channel morphological diversity over time. Regional implementation of the monitoring of channel morphology is planned for introduction in the 2007/08 financial year through the newly reviewed Fluvial Research Programme. The monitoring will be conducted in line with recommendations from this report. Kate McArthur Environmental Scientist – Water Quality Horizons Regional Council ii CONTENTS Foreword i Contents 3 1. -
Darcy's Law and Hydraulic Head
Darcy’s Law and Hydraulic Head 1. Hydraulic Head hh12− QK= A h L p1 h1 h2 h1 and h2 are hydraulic heads associated with hp2 points 1 and 2. Q The hydraulic head, or z1 total head, is a measure z2 of the potential of the datum water fluid at the measurement point. “Potential of a fluid at a specific point is the work required to transform a unit of mass of fluid from an arbitrarily chosen state to the state under consideration.” Three Types of Potentials A. Pressure potential work required to raise the water pressure 1 P 1 P m P W1 = VdP = dP = ∫0 ∫0 m m ρ w ρ w ρw : density of water assumed to be independent of pressure V: volume z = z P = P v = v Current state z = 0 P = 0 v = 0 Reference state B. Elevation potential work required to raise the elevation 1 Z W ==mgdz gz 2 m ∫0 C. Kinetic potential work required to raise the velocity (dz = vdt) 2 11ZZdv vv W ==madz m dz == vdv 3 m ∫∫∫00m dt 02 Total potential: Total [hydraulic] head: P v 2 Φ P v 2 h == ++z Φ= +gz + g ρ g 2g ρw 2 w Unit [L2T-1] Unit [L] 2 Total head or P v hydraulic head: h =++z ρw g 2g Kinetic term pressure elevation [L] head [L] Piezometer P1 P2 ρg ρg h1 h2 z1 z2 datum A fluid moves from where the total head is higher to where it is lower. For an ideal fluid (frictionless and incompressible), the total head would stay constant.