ASTM D4106-1996(2002) Standard Test Method (Analytical Procedure) for Determining Transmissivity and Storage Coefficient of Nonleaky Confined Aquifers by the Theis Nonequilibrium M.pdf
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1、Designation: D 4106 96 (Reapproved 2002)Standard Test Method(Analytical Procedure) for Determining Transmissivity andStorage Coefficient of Nonleaky Confined Aquifers by theTheis Nonequilibrium Method1This standard is issued under the fixed designation D 4106; the number immediately following the de
2、signation indicates the year oforiginal adoption or, in the case of revision, the year of last revision. A number in parentheses indicates the year of last reapproval. Asuperscript epsilon (e) indicates an editorial change since the last revision or reapproval.1. Scope1.1 This test method covers an
3、analytical procedure fordetermining the transmissivity and storage coefficient of anonleaky confined aquifer. It is used to analyze data onwater-level response collected during radial flow to or from awell of constant discharge or injection.1.2 This analytical procedure is used in conjunction with t
4、hefield procedure given in Test Method D 4050.1.3 LimitationsThe limitations of this test method fordetermination of hydraulic properties of aquifers are primarilyrelated to the correspondence between the field situation andthe simplifying assumptions of this test method (see 5.1).1.4 The values sta
5、ted in SI units are to be regarded asstandard.1.5 This standard does not purport to address all of thesafety concerns, if any, associated with its use. It is theresponsibility of the user of this standard to establish appro-priate safety and health practices and determine the applica-bility of regul
6、atory limitations prior to use.2. Referenced Documents2.1 ASTM Standards:D 653 Terminology Relating to Soil, Rock, and ContainedFluids2D 4043 Guide for Selection of Aquifer Test Method inDetermining of Hydraulic Properties by Well Techniques2D 4050 Test Method (Field Procedure) for Withdrawal andInj
7、ection Well Tests for Determining Hydraulic Propertiesof Aquifer Systems23. Terminology3.1 Definitions:3.1.1 aquifer, confinedan aquifer bounded above andbelow by confining beds and in which the static head is abovethe top of the aquifer.3.1.2 confining beda hydrogeologic unit of less perme-able mat
8、erial bounding one or more aquifers.3.1.3 control wellwell by which the head and flow in theaquifer is changed, for example, by pumping, injection, orimposing a constant change of head.3.1.4 drawdownvertical distance the static head is low-ered due to the removal of water.3.1.5 headsee head, static.
9、3.1.6 head, staticthe height above a standard datum of thesurface of a column of water (or other liquid) that can besupported by the static pressure at a given point.3.1.7 hydraulic conductivity (field aquifer tests)the vol-ume of water at the existing kinematic viscosity that will movein a unit tim
10、e under a unit hydraulic gradient through a unitarea measured at right angles to the direction of flow.3.1.8 observation wella well open to all or part of anaquifer.3.1.9 piezometera device so constructed and sealed as tomeasure hydraulic head at a point in the subsurface.3.1.10 specific storagethe
11、volume of water released fromor taken into storage per unit volume of the porous medium perunit change in head.3.1.11 storage coeffcientthe volume of water an aquiferreleases from or takes into storage per unit surface area of theaquifer per unit change in head. For a confined aquifer, thestorage co
12、efficient is equal to the product of the specific storageand aquifer thickness. For an unconfined aquifer, the storagecoefficient is approximately equal to the specific yield.3.1.12 transmissivitythe volume of water at the existingkinematic viscosity that will move in a unit time under a unithydraul
13、ic gradient through a unit width of the aquifer.3.1.13 unconfined aquiferan aquifer that has a watertable.3.1.14 For definitions of other terms used in this testmethod, see Terminology D 653.3.2 Symbols:Symbols and Dimensions:3.2.1 K LT1hydraulic conductivity.3.2.2 Kxyhydraulic conductivity in the h
14、orizontal plane,radially from the control well.3.2.3 Kzhydraulic conductivity in the vertical direction.3.2.4 Q L3T1discharge.3.2.5 S ndstorage coefficient.3.2.6 SsL1specific storage.1This test method is under the jurisdiction of ASTM Committee D18 on Soil andRock and is the direct responsibility of
15、 Subcommittee D18.21 on Ground Water andVadose Zone Investigations.Current edition approved Oct. 10, 1996. Published June 1997. Originallypublished as D 4106 91.2Annual Book of ASTM Standards, Vol 04.08.1Copyright ASTM International, 100 Barr Harbor Drive, PO Box C700, West Conshohocken, PA 19428-29
16、59, United States.3.2.7 T L2T1transmissivity.3.2.8 W(u) ndwell function of u.3.2.9 b Lthickness of aquifer.3.2.10 r Lradial distance from control well.3.2.11 s Ldrawdown.4. Summary of Test Method4.1 This test method describes an analytical procedure foranalyzing data collected during a withdrawal or
17、 injection welltest. The field procedure (see Test Method D 4050) involvespumping a control well at a constant rate and measuring thewater level response in one or more observation wells orpiezometers. The water-level response in the aquifer is afunction of the transmissivity and storage coefficient
18、 of theaquifer. Alternatively, this test method can be performed byinjecting water at a constant rate into the aquifer through thecontrol well. Analysis of buildup of water level in response toinjection is similar to analysis of drawdown of water level inresponse to withdrawal in a confined aquifer.
19、 Drawdown ofwater level is analyzed by plotting drawdown against factorsincorporating either time or distance from the control well, orboth, and matching the drawdown response with a type curve.4.2 SolutionThe solution given by Theis (1)3may beexpressed as follows:s 5Q4pT*u e2yydy (1)where:u 5r2S4Tt
20、(2)*u e2yydy 5 Wu!520.577216 2 logeu 1 u 2u22!21u33!32u44!41 .(3)5. Significance and Use5.1 Assumptions:5.1.1 Well discharges at a constant rate, Q.5.1.2 Well is of infinitesimal diameter and fully penetratesthe aquifer.5.1.3 The nonleaky aquifer is homogeneous, isotropic, andaerially extensive. A n
21、onleaky aquifer receives insignificantcontribution of water from confining beds.5.1.4 Discharge from the well is derived exclusively fromstorage in the aquifer.5.1.5 The geometry of the assumed aquifer and well condi-tions are shown in Fig. 1.5.2 Implications of Assumptions:5.2.1 Implicit in the ass
22、umptions are the conditions of radialflow. Vertical flow components are induced by a control wellthat partially penetrates the aquifer, that is, the well is not opento the aquifer through its full thickness. If the control well doesnot fully penetrate the aquifer, the nearest piezometer orpartially
23、penetrating observation well should be located at adistance, r, beyond which vertical flow components are negli-gible, where according to Reed (2):r 5 1.5bKzKxy(4)This section applies to distance-drawdown calculations oftransmissivity and storage coefficient and time-drawdown cal-culations of storag
24、e coefficient. If possible, compute transmis-sivity from time-drawdown data from wells located within adistance, r, of the pumped well using data measured after theeffects of partial penetration have become constant. The time atwhich this occurs is given by Hantush (3) by:t 5 b2s/2T Kz/Kr! (5)Fully
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