fluvial Hydrosystems
`
`Edited by
`
`G. E. Petts
`
`School of Geography
`University of Birmingham
`Birmingham, UK
`
`and
`
`C. Amoros
`
`Universite Claude-Bernard
`Ecologie des Eaux Douces et des Grands Fleuves
`Lyon, France
`
`CHAPMAN & HALL
`London · W einheim · New York ·Tokyo · Melbourne· Madras
`
`Page 1 of 4
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`PETITIONERS’ EXHIBIT 1141
`TOYOTA AND AISIN v. IV
`IPR2017-01494
`
`

`

`Published by Chapman & Hall, 2-6 Boundary Row, London SEl BHN, UK
`
`Chapman & Hall, 2- 6 Boundary Row, London SEl 8HN, UK
`
`Chapman & Hall GmbH, Pappelallee 3, 69469 Weinheim, Germany
`
`Chapman & Hall USA, l15 Fifth Avenue, New York, NY 10003, USA
`
`Chapman & Hall Japan, ITP-Japan, Kyowa Building, 3F, 2-2-1 Hirakawacho,
`Chiyoda-ku, Tokyo 102, Japan
`
`Chapman & Hall Australia, 102 Dodds Street, South Melboume, Victoria 3205,
`Australia
`
`Contents
`
`Chapman & Hall fndia, R. Seshadri, 32 Second Main Road, CIT East, Madras
`600 035, India
`
`List of contributors
`Preface and acknowledgements
`
`1 The fluvial hydrosystem
`G. E. Petts and C. Amoros
`1.1 The background
`1.2 Traditional approaches
`1.3 The fluvial hydrosystem approach
`
`2 A drainage basin perspective
`G. E. Petts and J.-P. Bravard
`2.1 The context
`2.2 Source area characteristics
`2.3 Large basins
`2.4 Basin history
`2.5 Biological responses
`2.6 The fluvial hydrosystem approach
`
`3 Hydrological and hydrochemical dynamics
`R. Wilby and J. Gibert
`3.1 Introduction
`3.2 Headwater streams
`3.3 Large rivers
`3.4 Concluding remarks
`
`4 Geomorphology of temperate rivers
`D. Gilvear and J.-P. Bravard
`4.1 Introduction
`4.2 Fundamental principles
`
`ix
`xi
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`1
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`1
`2
`5
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`13
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`19
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`35
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`-
`, r 5 f {) /) (p
`} ~:/:;;
`j
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`' f 7.'
`
`First published Hydrosystemiemes Fluviaux.
`First edition 1996
`© 19% Chapman & Hall
`Phototypeset in 10/12pt Palatino by fntype London Ltd
`Printed in Great Britain by St Edmundsbury Press, Bury St. Edmunds, Suffolk
`
`ISBN O 412 37100 6
`
`Apart from any fair dealing for the purposes of research or private study, or
`criticism or review, as permitted under the UK Copyright Designs and Patents
`Act 1988, this publicMion may not be reproduced, stored, or transmitted, in
`any form or by any means, without the prior permission in writing of the
`publishers, or in the case of reprographic reproduction only in accordance with
`the terms of the licences issued by the Copyright Licensing Agency in the
`UK, or in accordance with the terms of licences issued by the appropriate
`l~eproduction Rights Organization outside the UK.
`Enquiries concerning reproduction outside the terms stated here should be
`sent to the publishers at the London address printed on this page,
`The publisher makes no representation, express or implied, with regard to
`the accuracy of the infc,rrnation contained in this book and cannot accept any
`legal responsibility or liability for any errors or omissions that may be made.
`
`A catalogue record for this book is available from the British Library
`
`Library of Congress Catalog Card Number: 96-84806
`
`00 Printed on permanent acid-free text paper, manufactured in accordance
`with ANSI/NISO Z3'l.48- 19'l2 and ANSI/NISO Z3'l.48- 1g84 (Permanence of
`Paper) .
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`Page 2 of 4
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`Contents vii
`
`10.2 Modes and mechanisms
`10.3 Stability and different spatial and temporal scales
`
`11 Human impacts on fluvial hydrosystems
`J.-P. Bravard and G. E. Petts
`11.1 Catchment scale impacts
`11.2 Direct impacts on river beds
`11.3 The impact of dams on fluvial hydrosystems
`11.4 Complex impacts on hydrosystems
`
`12 Fluvial hydrosystems: a management perspective
`G. E. Petts and C. Amoros
`12.l Background
`12.2 Rationale for river rehabilitation
`12.3 The scientific basis
`12.4 Options for managing fluvial hydrosystems
`12.5 Catchment management
`12.6 Conclusion
`
`References
`
`I11dex
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`215
`238
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`242
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`242
`245
`251
`259
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`263
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`265
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`270
`276
`278
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`279
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`307
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`vi Contents
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`4.3 Channel adjustment
`4.4 The longitudinal dimension
`4.5 The vertical dimension
`4.6 The transverse dimension
`4.7 Valley fills and floodplain sedimentology
`
`5 Hydrological and geomorphological structure of hydrostreams
`J.-P. Bravard and D. J. Gilvear
`5.1 Introduction
`5.2 The main types of functional sector
`5.3 Patchwork dynamics
`
`6 Primary production and primary producers
`A R. G. Large, G. Pautou and C. Amoros
`6.1 Introduction
`6.2 Adaptive strategies
`6.3 Distribution and production
`6.4 Conclusion
`
`7 Aquatic invertebrates
`M. T. Greenwood and M. Richardot-Coulet
`7.1 Introduction
`7.2 Longitudinal patterns: macroscnle
`7.3 Spatial variation within functional sectors: mesoscale
`7.4 Spatial variation within each functional unit: microscale
`7.5 Temporal dynamics
`7.6 Conclusion
`
`8 Fish populations in rivers
`A L. Roux and G. H . Copp
`8.1 Introduction
`8.2 The longitudinal zonation of watercourses
`8.3 Use of floodplain biotopes by fish
`8.4 The impacts of river management schemes
`
`9 Interactions between units of the fluvial hydrosystem
`C. Amoros, J. Gibert and M. T. Greenwood
`9.1 Introduction
`9.2 Nature and effect of exchanges and interactions
`9.3 Topological effects
`9.4 Connectivity and temporal variations
`
`10 Ecological successions
`C. Amoros and P. M . Wade
`10.1 Definitions and concepts
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`75
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`Page 3 of 4
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`72 Geomorphology of temperate rivers
`
`Fundamental principles 73
`
`p
`
`where V is mean water velocity, R is hydraulic radius, S channel bed
`slope and Manning's 'n' is a measure of channel roughness. The hydraulic
`radius is the wetted cross-sectional area (A) divided by wetted perimeter
`(WP) and approximates to mean depth (d) (Table 4.1). Indices of bed
`grain size are usually used to quantify channel roughness (Table 4.1),
`but defining a representative value Jor heterogeneous bed material is
`problematic since larger particles have a greater effect on roughness than
`small particles. Representative values of Manning's 'n' have been defined
`for channels of different character and using descriptive tables these can
`be applied to similar channels but at best they will only be an approxi(cid:173)
`mation of roughness (Petts and Foster, 1985 and Gregory and Walling,
`1973 give representative Manning's 'n' values). Ignoring the roughness
`factor the open channel flow equation is effectively a depth-slope prod(cid:173)
`uct and the Chezy coefficient relates mean velocity to the square root of
`the 'depth-slope' product.
`
`V = c(RS)0.s
`where c is the Chezy coefficient.
`The depth-slope product also appears in the equation for the tractive
`force or shear force exerted on the river-bed (T) a major factor determin(cid:173)
`ing sediment entrainment;
`) = gyds
`µ(Newtons m-2
`where g is the gravitional constant, y is the specific weight of water, d is
`depth and s is slope.
`
`4.2.2 TYPES OF FLOW
`
`Several types offlow are theoretically possible in open channels: uniform,
`non-uniform, steady, laminar, turbulent, tranquil and rapid flow. In
`reality only a number occur. For example, uniform flow describes flow
`where there is no change with distance in either magnitude or velocity
`along a flowline but in reality variations in velocity in space and time
`occur and non-uniform flow exists. Similarly steady flow relates to no
`velocity change with time, but in reality, changes in discharge result
`in velocity fluctuations. Flow in rivers is therefore generally non-uniform
`and unsteady.
`The existence of laminar flow or turbulent flow depends on the Reyn(cid:173)
`olds number (Re), an index of flow turbulence, where:
`
`Re=~
`u
`
`where pis water density and u is dynamic viscosity. This is a dimension(cid:173)
`less ratio of the inertial to the viscous forces. Laminar flow occurs when
`viscous forces predominate but generally speaking laminar flow rarely
`occurs in rivers. Turbulent flow occurs when inertial forces are large in
`comparison to viscous forces. Diffusion takes place by groups of mole(cid:173)
`cules and gives rise to additional viscous resistance termed the eddy
`viscosity.
`The criterion for tranquil flow and rapid turbulent flow is the Froude
`(Fr) number which is a dimensionless ratio of inertial to gravity forces:
`
`Fr =-v-
`(gd)o.s
`
`When the Froude number is less than 1, flow is tranquil; when it is equal
`to 1 flow is critical and when it exceeds 1 it is rapid. Flow is normally
`tranquil.
`
`4.2.3 STREAM POWER
`
`One of the most important expressions of the hydraulics of channel flow
`is 'stream power' which is the work expended or energy loss. Stream
`power is therefore a key parameter in controlling erosion and sediment
`transport and possibly as a control on aquatic biotopes.
`Stream power (W m-1) = yQs
`where Q = stream discharge in m 3s -1 or Is- 1
`•
`Ferguson (1981) showed that stream power at bankfull discharge in
`British rivers has a 1000-fold range. Unit stream power (P) is an important
`dimensionless index for comparative studies.
`
`P (dyn s-1) = uQ§.
`w
`
`where w is channel width. Stream power varies as the cube of velocity,
`and thus slight changes in velocity can significantly affect potential
`stream power.
`
`4.2.4 TIIE CONTINUITY EQUATION
`
`In any given reach, in the absence of water inputs, the volume of water
`moving through a cross~section, even if it is radically different in size,
`slope or shape from the cross-section immediately above, must equal the
`amount of water being conveyed from upstream. Thus, the product of
`the mean velocity of flow and cross-sectional area at the downstream
`cross-section must equal the product of cross-sectional ·area and mean
`velocity of flow upstream (i.e. A1 V1 = A2V2). This simple algorithm is
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`Page 4 of 4
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