Optically stimulated luminescence dating of fluvial deposits: a review

Optically stimulated luminescence dating of uvial deposits a review

JAKOB WALLINGA

Wallinga J 2002 (December) Optically stimulated luminescence dating of uvial deposits a review BoreasVol 31 pp 303ndash322 Oslo ISSN 0300-9483

Optically Stimulated Luminescence (OSL) dating allows age determination of sediments deposited during the lastglacialndashinterglacial cycle This relatively new technique therefore enables chronological frameworks to beestablished for uvial deposits that often cannot be dated by other means The OSL signal of quartz and feldsparminerals is reset by light exposure during uvial transport and builds up as a result of ionizing radiation afterburial of the minerals Incomplete resetting of the OSL signal because of inadequate light exposure in the uvialenvironment can result in age overestimations especially for relatively young samples Methods used for thedetection of incomplete resetting or poor bleaching are reviewed It is argued that techniques measuring the OSLsignal from small subsamples (aliquots) are most promising for detecting poor bleaching and for obtaining thetrue age for a sample in which not all grains had their OSL signal completely removed at deposition Quartzshould be the mineral of choice because it has been shown to yield the most reliable results and because its OSLsignal is more rapidly reset than that of feldspar Aliquot size should be small with aliquots ideally consisting of asingle grain of quartz for samples in which the majority of grains are poorly bleached Using single-aliquot datingof coarse-grain quartz age offsets between zero and a few thousand years have been found for modern uvialdeposits The validity of single-aliquot quartz OSL dating has been demonstrated by application to known-agesamples but for the older age range (gtsup113 ka) further proof of the accuracy of the method is essential Theapplication of quartz OSL dating to investigations of uvial deposits opens a new realm of possibilities to beexplored as is highlighted by some examples of geological applications

Jakob Wallinga (e-mail jwallingairitudelftnl) The Netherlands Centre for Geo-ecological Research(ICG) Faculty of Geographical Sciences Utrecht University PO Box 80115 NL-3508 TC Utrecht TheNetherlands present address Netherlands Centre for Luminescence Dating (NCL being established) IRIDelft University of Technology Mekelweg 15 NL-2629 JB Delft The Netherlands received 22nd October2001 accepted 23rd April 2002

Rivers are among the worldrsquos most important geo-morphic agents (eg Vandenberghe amp Maddy 2000)and respond to tectonic movements and changes inclimate and sea level (eg Blum amp Tornqvist 2000) Animproved understanding of uvial response to externalforcing is particularly important in the light of climaticand sea-level changes induced by greenhouse effects soit is not surprising that uvial deposits receive abundantattention from geologists geomorphologists strati-graphers and sedimentologists However age determi-nation of uvial deposits can be problematic (seeSowers et al 2000 Stokes amp Walling in press) Radio-carbon dating the most widely used geochronologicaltool is often not applicable because of the lack of in situorganic material and the limited age range (ltsup135 ka)covered by this method Other techniques based onradioactive decay (eg uranium series potassium-argon) are rarely applicable to uvial deposits

The timing of the last exposure to light of quartz andfeldspar minerals (the main constituents of sand andsilt) can be determined with luminescence datingtechniques Although originally mainly applied toaeolian deposits the technique is now increasinglyused to determine the timing of deposition of uvialsediments However the assumption in luminescencedating that the signal is completely zeroed prior todeposition is arguable for uvial deposits owing to thelimited light exposure of sediment grains during

transport Incomplete zeroing results in an overestima-tion of age and has prevented widespread use ofthermoluminescence (TL) dating for uvial depositsThe Optically Stimulated Luminescence (OSL) signalthat is now used is more sensitive to light and istherefore more suitable for the dating of uvialsediments This technique is known as OSL or opticaldating (see recent reviews by Duller (1996) Aitken(1998) and Stokes (1999))

In his review of the dating of Quaternary sedimentsDuller (1996) stated that lsquothe development of OSL-dating methods has had a profound effect upon the eldenabling younger materials to be dated increasing thediversity of depositional environments that can bedated and allowing the development of novelmethods of age determinationrsquo In the years sincepublication of Dullerrsquos paper improved proceduresfor OSL dating have resulted in the establishment of thisdating technique As a result the application of OSLdating to uvial deposits has increased rapidly Hencethe time is right for a review discussing recentdevelopments in OSL dating This review focuses on uvial deposits because of the importance of uvialdeposits in the geological record and the speci cchallenges encountered when applying OSL dating to uvial sediments

The aim of this paper is to assess the suitability ofOSL dating techniques for establishing accurate chron-

2002 Taylor amp Francis

ologies for uvial deposits The paper is addressed tothe user community wishing to use OSL dating tech-niques to establish the chronology of ( uvial) depositsas well as to the OSL dating community The paperdescribes and discusses the methods and proceduresused for OSL dating Much attention is given to thedetection of incomplete resetting of the luminescencesignal prior to deposition because of its relevance to theOSL dating of uvial deposits The validity of the OSLages is discussed by reviewing OSL dating results on uvial deposits of known chronology many of whichare modern Finally examples are discussed of geo-logical applications of OSL dating to uvial deposits ofunknown chronology

Luminescence dating

After sedimentation grains of quartz and feldspar areburied and exposed to low-level ionizing radiationwhich is produced by the decay of naturally occurringradionuclides (mainly of the U and Th series and 40K)and a in most cases relatively small contribution fromcosmic rays During this exposure to ionizing radiationfree charge carriers (electrons and holes) are producedand some of them are trapped at defects in the crystallattice (Fig 1) Charge trapped in the OSL traps is stableover long periods of time but is released when themineral is exposed to light Hence the total amount ofcharge in these traps will increase with burial time but

the charge is released when the mineral grains areeroded and transported in daylight Thus the amount oftrapped charge forms a clock that starts ticking from themoment the mineral is buried and shielded from light

Luminescence dating makes use of the physicalphenomenon of luminescence a very small light uxresulting from the recombination of electrons releasedfrom traps and holes Recombination can be forcedeither by heating the mineral (TL) or by exposing it tolight (OSL) The brightness of the luminescence signalre ects the amount of charge trapped and hence theirradiation dose the sample has received since burial(equivalent dose) The age of a sample is given by thefollowing equation where the annual dose is theirradiation dose ux in the natural environment

Age(a) ˆ equivalent dose (Gy)annual dose (Gya)

Luminescence dating allows determination of abso-lute ages in the range of years to one million years Atthe lower end of the age range the technique is limitedby incomplete resetting of the OSL signal prior todeposition this will be discussed in detail in the nextsection The maximum age for application of OSLdating is determined by saturation of the traps in thecrystal For quartz this usually limits its application tothe last 150 ka whereas for feldspar dating up to 1 Ma ispossible in principal The precision of age estimationsfor sediments with low luminescence sensitivity can belimited by the dimness of the luminescence signal thisapplies especially in the case of young deposits

A wide range of measurement procedures is used forequivalent-dose determination of both quartz andfeldspar separates In this section the general termsare explained Wintle (1997) Aitken (1998) andMurray amp Wintle (2000) provide a full accountEquivalent-dose determination involves establishinghow much radiation exposure is needed to obtain anOSL signal identical to that resulting from naturalradiation exposure

In traditional methods (the multiple-aliquot proce-dures) a number of aliquots (subsamples each contain-ing a few hundred to a few thousand grains 2ndash15 mg ofmaterial) are prepared and divided into groups eachcontaining at least three aliquots One group is used formeasurement of the natural OSL signal The othergroups are given various doses either on top of theirnatural dose (for additive-dose procedures) or afterexposure to light (for regenerative-dose procedures) Adose-response curve is constructed from measurementson each group and the equivalent dose is obtained byextrapolation of this curve (in additive-dose proce-dures) or by projection of the natural OSL signal on thiscurve (in regenerative-dose procedures) (Fig 2) Dis-advantages of multiple-aliquot procedures are thatnormalization is needed to account for aliquot-to-aliquot differences in luminescence sensitivity and

Fig 1 Simpli ed energy-level diagram showing the electron andhole transitions that are responsible for the occurrence of OSL(redrawn from Aitken 1998 p 14) A At exposure of the crystal toradiation ionization results in the trapping of electrons and holes atdefects T and L respectively B To be used for dating the lifetime ofthe electrons in the traps needs to be at least several million yearsThis is the case for traps giving rise to the quartz OSL signal CExposure to light of the appropriate wavelength will evict electronsfrom traps Subsequent recombination with holes trapped atluminescence centres will give rise to the emission of a minute lightemission called optically stimulated luminescence

304 Jakob Wallinga BOREAS 31 (2002)

that a large number of aliquots is needed for equivalent-dose determination

To overcome the problems with multiple-aliquotmethods single-aliquot procedures have been devel-oped (Duller 1991) These allow determination of theequivalent dose on a single aliquot by making repeatedmeasurements of its OSL signal intensity In single-aliquot additive-dose procedures short measurementsof the OSL signal are made leaving the majority oftrapped charge in place Corrections are made for theloss in trapped charge due the OSL measurements andfor the loss due to heating of the sample during the

procedure In single-aliquot regenerative-dose proce-dures all light-sensitive trapped charge is removedduring the OSL measurements Initial attempts to usesingle-aliquot regenerative-dose procedures failed dueto sensitivity changes during measurement but theseproblems are largely overcome in the recently devel-oped Single-Aliquot Regenerative-dose (SAR) protocol(Murray amp Roberts 1998 Murray amp Wintle 2000)Single-aliquot methods can be used to measure theequivalent dose of single grains of sand (by reducing thealiquot size to a single grain) which is of interest for thedating of uvial deposits as will be discussed below

Resetting the OSL signal

In full sunlight the trapped charge sampled in OSLmeasurements for dating is reduced by a factor of 10 ina time span of seconds to minutes (Godfrey-Smith et al1988 reproduced in Fig 3) this process of de-trappingcharge by light exposure is normally referred to asbleaching or zeroing Under turbid water in a uvialenvironment the intensity of the light is greatly reducedand the spectrum of the light is restricted (eg Berger ampLuternauer 1987 reproduced in Fig 4) As a conse-quence some trapped charge might remain at the timeof deposition and burial of the grains As luminescencemeasurements cannot distinguish between chargetrapped before and after burial such remaining trappedcharge may lead to a signi cant overestimation of theluminescence age

Duller (1994) distinguished two types of poor

Fig 2 Graphic representation of the additive-dose (A) and theregenerative-dose (B) procedures (redrawn from Aitken 1998 pp12ndash13) In additive-dose procedures the equivalent dose (De) isobtained by extrapolation of the dose-response curve which isobtained by exposing natural aliquots to radiation and subsequentmeasurement of the OSL signal resulting from the combined naturaland added dose In regenerative-dose procedures the equivalent doseis obtained by projection of the natural OSL signal (N) onto the dose-response curve which is obtained by exposing bleached aliquots toradiation and measurement of the OSL signal resulting from thislaboratory dose

Fig 3 Sunlight bleaching of natural TL and of natural OSL (redrawnfrom Godfrey-Smith et al 1988) Quartz grains (q) and K-feldspargrains (f) were used the unbleached luminescence levels are shownon the vertical axis The graph shows that the OSL of the minerals( and Dagger) is reset more readily than the TL ( and ~) It is alsoshown that the quartz OSL is reset more quickly than the feldsparOSL Details on the experimental procedure are given in Godfrey-Smith et al (1988) and Aitken (1998 p 19)

BOREAS 31 (2002) Optically stimulated luminescence dating of uvial deposits 305

bleaching In the rst type all the grains are poorlybleached to the same degree and each grain will havethe same level of trapped charge at the time ofdeposition if the grains had been measured at deposi-tion the lsquorelic OSLrsquo would have given rise to ameasurable equivalent dose In the second type it washypothesized that the grains were optically bleached todifferent degrees and OSL measurements on each grainwould give a different equivalent dose Uniformbleaching in the natural environment is unlikely owingto grain-to-grain variations in previous dose bleach-ability variation in light-absorbent coatings and varia-tion in duration of bleaching (Aitken 1998 p 154)Therefore it is widely assumed that the only feasibleway of creating a deposit containing uniformly bleachedgrains that overestimate the age of deposition (ie the rst type of poor bleaching) is by the incorporation ofgrains from an older deposit by means of a process thatprecludes light exposure Such could be the case whenfor example all the grains are from the same source andtransported during a single event at night or in highlatitude environments during the polar winter Suchdeposits are likely to be rare and most poorly bleachedsediments will almost certainly consist of a mixture ofpoorly bleached and well-bleached grains

The above discussion focuses on age offsets as aconsequence of charge remaining in the OSL trap afterbleaching However charge remaining in relativelylight-insensitive traps after bleaching can also give riseto an age overestimation as a consequence of thermaltransfer Prior to measurement samples are normallyheated to allow direct comparison of the natural OSL

signal with that after laboratory irradiation Preheatingis thought to be needed to empty thermally shallow(=unstable) traps and to transfer charge from thesetraps into the deeper stable traps For the natural doseboth processes have already occurred at ambient tem-perature during geological time but this is not the casefor a dose administered in the laboratory Unfortunatelyapart from this desired charge transfer by heating(thermal transfer) there is also the possibility oftransferring charge from poorly bleached light-insensi-tive traps into the light-sensitive trap sampled in theOSL procedure This has been reported for infraredstimulated luminescence (IR-OSL) from feldsparrecently derived from nearshore environments (Huntleyamp Clague 1996 Richardson 2000) Although thermaltransfer might not be as important for quartz aspreviously thought (see discussion in Wintle amp Murray2000) it can cause signi cant offsets in equivalent dosewhen the amount of charge in the light-insensitive trapsis far greater than that in the light-sensitive traps(Rhodes 2000)

Detection of poor bleaching

In applying OSL dating it is important to assesswhether the light-sensitive trapped charge of everygrain was zeroed prior to deposition If such is the casethe age of the deposit can be obtained using OSL datingof any number of grains If not special care has to betaken to use only the OSL signal from those grains thathad their charge zeroed (if available) or alternativelythe age obtained should be interpreted as a maximumage for the deposits

Methods that have been proposed to detect incom-plete resetting of the OSL signal can be divided intothree categories based on (1) the scatter in OSL results(2) the form of the optical decay curve (3) comparisonof different luminescence signals The three methodstheir applications and their limitations are discussedhere

Scatter in OSL results

Grain-to-grain variations in equivalent dose will pro-duce scatter in results obtained by multiple-aliquot(Rhodes 1990 Duller 1994 Huntley amp Berger 1995)and single-aliquot (Li 1994 Clarke 1996 Clarke et al1999) methods In the former scatter is observed forduplicated dose points on the growth curve even afterapplication of a normalization procedure In the latterscatter is observed in the values of the equivalent doseobtained for multiple determinations The existence ofscatter is a clear indication that the sample under studymight be incompletely bleached (Wallinga 2002)although other sources of scatter (eg micro-dosimetry)cannot be ruled out (Murray amp Roberts 1997 Olley etal 1997)

Fig 4 The light spectrum at the surface (dotted) and at 4-m depth(dashed) in a turbid river (redrawn from Berger amp Luternauer 1987)Note that the light spectrum at 4-m depth has been multiplied by5 pound 104 () to allow plotting on the same scale The bleachingef ciency of quartz (solid circles data taken from Spooner 1994a)and feldspar (open circles data taken from Spooner 1994b) is alsoshown Combination of the information on light spectrum in a turbidriver and bleaching of quartz and feldspar minerals suggests thatfeldspar is bleached more readily in such an environment Howeverthe extremely low light intensity makes it unlikely that anysigni cant bleaching takes place near the bottom of a turbid river


Thresholds based on the existence of scatter inequivalent doses obtained by single-aliquot techniqueshave been suggested as a means of detecting poorbleaching (Clarke 1996) and of ensuring that a sample iswell bleached (Clarke et al 1999) However the degreeof scatter is largely dependent on the number of grainsper aliquot (eg Li 1994) and the type of mixture ofwell-bleached and poorly bleached grains (Olley et al1999 Wallinga 2002) which makes the use of thresh-olds impossible It has also been suggested that anincreasing trend of the equivalent dose with the aliquotnatural OSL intensity is an indication of poor bleaching(Li 1994 Colls et al 2001 Stokes et al 2001) withplots of the two parameters being used as a visual check(Fig 5) However such a trend yields no informationwhether inhomogeneous bleaching causes the observedscatter in equivalent dose A clear trend merely demon-strates that scatter in equivalent dose is the main causefor scatter in natural OSL intensities Such is to beexpected if the luminescence sensitivity of the grains isrelatively homogeneous (Wallinga 2002) which is theexception rather than the rule in natural samples

Other types for graphical presentation suggested fordetection of poor bleaching include frequency histo-grams (Murray et al 1995 Olley et al 1998 1999reproduced in Fig 6) and radial plots (Galbraith 1990Olley et al 1999 reproduced in Fig 7) of equivalent

doses obtained by single-aliquot techniques Asymme-try of the histogram (with a tail to high equivalentdoses) points to contamination with a small percentageof poorly bleached grains (Olley et al 1998 1999)Lepper et al (2000) suggested a way to quantify thisasymmetry For all methods based on the scatter inequivalent doses it is important that the number ofgrains on each aliquot is relatively small to avoidaveraging of the equivalent dose within each aliquot(Olley et al 1999 Wallinga 2002) Ultimately eachaliquot consists of a single grain of quartz (eg Murrayamp Roberts 1997 Olley et al 1999) or feldspar (Lamotheet al 1994)

Form of the optical decay curve

In the initial OSL work (Huntley et al 1985) it wassuggested that a rise in equivalent dose as a function ofOSL illumination time may be indicative of insuf cientsignal resetting prior to deposition (Fig 8) This is basedon the idea that the OSL signal measured with longerillumination time originates from traps that are moredif cult to empty optically For a partially bleachedsample these dif cult-to-bleach traps can be expectedto be less well reset than the easy-to-bleach traps priorto deposition and therefore the equivalent doseobtained from sampling the dif cult-to-bleach traps is

Fig 5 Graphs redrawn fromStokes et al (2001) used by theauthors to establish the degree ofbleaching for young samples fromthe Colorado River (USA)Equivalent doses of the quartzseparates were determined by thesingle-aliquot regenerative-dose(SAR) protocol using largealiquots The equivalent dosesobtained on the aliquots areplotted below the x-axis Theunweighted sample mean ( lledcircle above the x-axis) andassociated distribution are shownin the main graph The insetdiagrams show standardized plotsof the equivalent dose (De(z))versus aliquot intensity (I(z)) onthe base of which the authorsinterpret samples A and C to bepoorly bleached and samples Band D to be well bleached In themain text this method for poor-bleaching detection is criticallydiscussed


Fig 6 Frequency histograms ofequivalent doses obtained onsmall aliquots (60ndash100 grains) of uvial quartz (180ndash212 mm) fromAustralia (redrawn from Olley etal 1999) Graph A shows thedose distribution for a 70-year-oldsample (ME95041 see also Table1) whereas graph B shows thedistribution for a sup11500-year-oldsample (WK96008) Note thelarger offset from zero dose forthe latter The distributions areskewed to higher doses as aconsequence of contamination ofthe sample by a small number ofpoorly bleached grains

Fig 7 Radial plots for the same samples as in Fig 6 and also redrawn from Olley et al (1999) Radial plots allow plotting of each data pointwith its associated precision any radius passing through the origin represents a line of constant dose and the precision of the measurementincreases from left to right This graphical presentation allows visualization of dose distributions where focus will be drawn to the best-knownresults


expected to be higher In quartz traps have beenidenti ed with different decay constants giving rise tothe fast medium and slow components in the OSLsignal (Smith amp Rhodes 1994 Bailey et al 1997) eachcomponent is progressively more dif cult to bleach Fordating the easy-to-bleach trap giving rise to the fastOSL component is most suitable The dif cult-to-bleach traps giving rise to the slower OSL compo-nent(s) might never get completely zeroed even inideal bleaching conditions

Interpretation of equivalent-dose-versus-stimulation-time plots (De(t)-plots) has proven problematic inmultiple-aliquot procedures at De(t) plots have beenfound for poorly bleached samples (Stokes 1994)whereas a rising trend has been observed for well-bleached samples (Roberts et al 1994a b Bailey 2000)More promising results with De(t) plots have recentlybeen obtained by Bailey (pers comm) when using theSingle-Aliquot Regenerative-dose (SAR) protocol(Murray amp Wintle 2000) So far however onlylaboratory tests have been made and validity for natural

samples has not yet been demonstrated RecentlyLarsen et al (2000) suggested that the componentscan be better distinguished using linearly modulatedOSL (LM-OSL) a technique in which the stimulationpower is linearly increased during measurement (Bulur1996) Laboratory tests and computer simulationsindicate that using LM-OSL it is possible to recognizeincomplete bleaching of different OSL componentsafter controlled laboratory experiments (Larsen et al2000) but applicability for natural samples is yet to becon rmed

A related technique is the partial bleach methodinvestigated by Fuller et al (1994) for the IR-OSLdating of ne-grained overbank deposits from the RiverDanube in Romania In this multiple-aliquot proceduresets of aliquots are exposed to light after irradiationusing different exposure times for the sets The rationaleis that the IR-OSL signal measured after long exposuretimes is from hard-to-bleach traps only whereas the IR-OSL signal measured without prior light exposure isdominated by the easy-to-bleach traps However resultsobtained were unsatisfactory a rising trend of equiva-lent dose with exposure time was found for a uvialsample believed to be well bleached whereas nodependency was observed in poorly bleached samplecreated by laboratory bleaching (Fuller et al 1994)

As a concluding remark it should be noted that thesetechniques only detect differences between the degreeof bleaching of the fast OSL component relative to theslower components A difference between the signalsindicates that the slower components were not resetcompletely but yields no information on the degree ofbleaching of the fast component used for datingNevertheless it is clear that OSL dating measurementsshould aim at sampling only the easy-to-bleach traps toavoid problems with poor bleaching

Comparison of different luminescence signals

Comparison of luminescence signals with differentoptical decay constants yields some information onthe degree of bleaching If TL and OSL equivalentdoses are identical it can be assumed that the samplewas exposed to abundant light prior to depositionalthough an alternative explanation is that the samplewas not exposed to light This check for bleaching hasbeen used for feldspar (Fuller et al 1994) and quartz(Roberts et al 1994b) Recently Bluszcz (2001)proposed a method to measure the TL and OSLequivalent dose in a quartz sample in a single routine

The OSL signal from quartz is reset more quicklythan the infrared stimulated luminescence (IR-OSL)from feldspar when the minerals are exposed to sunlight(Godfrey-Smith et al 1988 Fig 3) In principle thisdifference in bleaching rate can be used to assesswhether the material was exposed to abundant lightprior to deposition (Fuller et al 1994) Hansen et al(1999) found feldspar IR-OSL ages to be greater than

Fig 8 In the original OSL work (Huntley et al 1985) it wasproposed that a rising trend of equivalent dose as a function ofstimulation time is an indication of incomplete bleaching Accordingto this method a 59 ka-old silt (A) and a 5 ka-old quartz (B) are wellbleached whereas a present-day beach sand (C) is identi ed aspoorly bleached Later work has shown that this approach is notreliable The graphs are redrawn from Huntley et al (1985)


quartz OSL ages for poorly bleached glacio uvialdeposits from Greenland However detailed studieson bleaching characteristics as a function of wavelengthhave shown great differences between quartz andfeldspar minerals (Spooner 1994a b respectively)The bleaching ef ciency of the minerals as a functionof wavelength is plotted in a single graph (Fig 4) toallow comparison for both mineral types Combiningthis information with information about the lightspectrum at 4 m depth in a turbid river (Berger ampLuternauer 1987) suggests that the feldspar IR-OSLsignal is reset more readily than the quartz OSL signalunder such light conditions However it is questionablewhether bleaching really takes place under thesecircumstances since the light intensity is extremelylow at these depths (sup1140000 of that at the surface) Itis therefore likely that most bleaching will occur whenthe grains are close to the water surface where the lightintensity is greater and the light spectrum is wider

From this discussion it follows that comparison ofquartz and feldspar OSL dating results yields nostraightforward indications on light exposure More-over it assumes that there are no problems other thanpoor bleaching associated with luminescence dating ofboth minerals which is a questionable assumption aswill be discussed later

Finally attempts have been made to infer the degreeof bleaching from differences in feldspar equivalentdoses obtained by using different stimulation anddetection wavelengths As different traps might be resetat different rates during light exposure in a uvialenvironment the stimulation and detection wavelengthsused could in uence how well bleached the sampleappears Since Balescu amp Lamothe (1992) showed thatthe IR-OSL signal detected in the UV region is lessstable than that in the blue region detection using blue lters has been generally adopted for equivalent-doseestimation on feldspar separates However it has beenargued that the signal detected in the UV would be resetmore rapidly Krause et al (1997) showed a depen-dency of IR-OSL age on the detection wavelength usedfor lacustrine sediments from Greenland They attrib-uted this to differences in rapidity of bleaching for thedifferent emission wavelengths but Preusser (1999b)later disputed this interpretation He found no signi -cant differences in bleaching ef ciency for IR-OSLemissions in the yellow blue and UV in laboratoryexperiments (Preusser 1999b) and for uvial samplesfrom Switzerland (Preusser 1999a)

With respect to the stimulation wavelength Spooner(1993) has shown that there is a hard-to-bleach com-ponent in feldspars that cannot be reset by wavelengthslonger than yellow This component is thus notstimulated by infrared light but it would be stimulatedif blue or green light were used for stimulation Wintle(1997) suggested that the differences in bleachingresponses of IR-OSL and blue-green-OSL could beused to identify poorly bleached samples If the blue-

green stimulated component is indeed more dif cult tobleach it is expected that the equivalent dose deter-mined using blue stimulated OSL is larger than thatdetermined using IR-OSL So far this suggestion hasnot been followed up for the detection of poor bleachingin natural samples Poolton et al (2002) recentlydemonstrated that the feldspar IR-OSL signalmeasured at elevated temperature is less well zeroedthan that measured at ambient temperature a featurethat could possibly be used for detection of poorbleaching

What method to use

Quartz versus feldspar

Rapidity of bleaching is an important attribute indeciding what mineral to use for the luminescencedating of uvial deposits As discussed in the previoussection quartz bleaches faster than feldspar in sunlightbut this might be reversed in a turbid river environment(see Fig 4) Hansen et al (1999) report feldspar IR-OSL ages a factor of 2 greater than quartz OSL ages forearly Holocene glacio uvial samples from East Green-land Comparisons of quartz and feldspar OSL ages on asubmodern uvial sample also showed a slightly lower(more accurate) age for the former (Wallinga et al2001) This evidence suggests that if there is adifference in the bleaching of quartz and feldspar in uvial environments the quartz OSL signal is likely tobe zeroed most effectively and is therefore the preferredmineral from this point of view Other importantattributes to decide what mineral should be the one ofchoice are the accuracy precision and age rangeavailable

Feldspar IR-OSL dating can be troubled by anom-alous fading (Wintle 1973 Spooner 1994b Lamothe ampAuclair 1999 Huntley amp Lamothe 2001) and changes intrapping sensitivity (Wallinga et al 2000) Bothphenomena are still poorly understood and correctionis problematic Methods for quartz OSL dating havegreatly improved over recent years since the launchingof the SAR method (Murray amp Roberts 1998) andsubsequent re nements (Murray amp Wintle 2000) In theSAR protocol sensitivity changes are monitored andcorrected and the procedure allows determination ofthe equivalent dose by interpolation Using the SARprotocol OSL ages have been obtained in goodagreement with independent age control for a widerange of depositional environments (see review byMurray amp Olley 2002) and a precision of better than5 is feasible The limitation of the application ofquartz OSL dating is the saturation of the quartz OSL atdoses of about 300 Gy which usually limits applic-ability to an age of about 150 ka depending on the doserate Nevertheless it is proposed that quartz should be


the mineral of choice for deposits where the quartz OSLsignal has not reached saturation

OSL dating of polymineral ne grains (4ndash11 mm)usually involves application of infrared stimulation toobtain a signal from the feldspar minerals in the sample(Aitken 1998) It is therefore likely to suffer from thesame problems as IR-OSL dating on sand-sized feldsparminerals Recently methods have been proposed(Banerjee et al 2001 Roberts amp Wintle 2001) to obtaina quartz-dominated OSL signal from polymineral ne-grains by measuring the blue-stimulated OSL signalafter exposure to infrared light So far however thesemethods have not been applied to uvial deposits

All in all OSL dating of sand-sized quartz using theSAR procedure is probably the best available methodfor luminescence dating of uvial deposits This reviewtherefore focuses on that method in the further discus-sion

Grain size

In a uvial environment ner grains are more likely tobe carried nearer the top of the water column thancoarser grains Fuller et al (1994) suggested that as aconsequence ner grains are more likely to bethoroughly exposed to light and thus better bleachedSurprisingly available information suggests the oppo-site to be true Olley et al (1998) were the rst to reportthat equivalent doses obtained on coarse quartz grainsyielded lower results than those obtained on ner grains(Fig 9) Similar results have since been reported byColls et al (2001) for two grain sizes from a modern uvial deposit from the Loire (France) For a uvialsample from the Rhine-Meuse system a strikingdependency of equivalent dose on grain size was found(Table 1) again with lowest (most accurate) resultsobtained on the coarsest grain size At this point one canonly speculate on the reasons for this behaviourNevertheless it seems fair to suggest that OSL datingof uvial deposits can bene t from using a relativelycoarse grain size for the equivalent-dose determination

The use of sand-sized grains instead of ne-grained(4ndash11 mm) material has the added advantage that OSLmeasurements can be made on aliquots containing fewgrains The extent of scatter in equivalent dosesobtained on these small aliquots allows inferences tobe drawn on the degree of bleaching of the deposit

Preheat

Preheating of quartz prior to measurement can result inthermal transfer from shallow light-insensitive traps tothe traps sampled during OSL measurement For a rangeof glacio uvial quartz samples preheating at 280degC for10 s caused thermal transfer resulting in an overesti-mation of the equivalent dose by up to 10 Gy (Rhodes2000 reproduced in Fig 10) Similar though lessdramatic thermal transfer was observed for uvial

quartz from the Rhine-Meuse delta in The Netherlands(Wallinga et al 2001)

Thermal transfer during preheating can be avoided byusing less stringent preheat regimes Use of a preheataround 200degC for 10 s yielded satisfactory results formodern quartz samples from glacio uvial (Rhodes2000) and uvial (Murray 1996 Stokes et al 2001Wallinga et al 2001) sediments However it is notguaranteed that such a preheating regime is also validfor older samples Firstly not only the unwanted butalso the lsquowantedrsquo component of thermal transfer isavoided which might give rise to age underestimationin older samples Extended preheat plateaus (egMurray amp Olley 1999) indicate that this is normallynot important but clearly more evidence is neededbefore adopting low preheats for older samplesSecondly unwanted thermal transfer can occur innature if the light-insensitive traps are thermallyunstable and part of their charge is retrapped in theOSL trap Such natural thermal transfer can cause anoverestimation of age and cannot be avoided by using alow preheat Therefore good results on modern sedi-

Fig 9 Grain-size dependency of the equivalent dose for anAustralian uvial quartz sample (ME95041 redrawn from Olley etal 1998) The apparent doses are plotted against the median particleradius for each size fraction A The apparent dose in 24 aliquots(each containing approximately 2000 grains) from 5 different grain-size fractions ranging from 63 to 250 mm B The means standarderrors (just larger than the symbol) and standard deviations of thedata presented in the top graph


ments are not a guarantee that results on older sampleswill be accurate as well

It is proposed that in dating uvial deposits it isessential to routinely use a wide range of preheat tem-peratures (eg a 10 s preheat at 7 temperatures from 150to 275degC) If a rising trend is observed the equivalentdoses obtained using the less-stringent preheats aremost likely to be accurate

Poor-bleaching detection

Although methods comparing equivalent doses ob-tained from different quartz OSL components (egLarsen et al 2000) seem promising their usefulness fornatural samples is yet to be con rmed Moreover thesemethods only compare the equivalent dose obtainedusing the fast OSL component to that from slower OSLcomponents Hence they cannot detect poor bleachingof the fast OSL component itself Therefore methodslooking at the scatter in equivalent doses obtained bysingle-aliquot methods seem to be the best way to detectpoor bleaching Aliquots need to be small to prevent

averaging of grain-to-grain variations in equivalentdose within the aliquot Measurement of single grainsis the ultimate method but unfortunately not alwaysfeasible For a well-bleached sample a tight symme-trical dose distribution is expected although widersymmetrical distributions are more often observed (egMurray et al 2002) A skewed dose distribution pointsto contamination with a small percentage of poorlybleached grains (Olley et al 1998 1999) whereasbroad distributions can be caused by an abundance ofpoorly bleached grains (Wallinga 2002) or by differ-ences in micro-dosimetry (Murray amp Roberts 1997Olley et al 1997)

Obtaining the true age from a poorly bleached sample

When the majority of the grains in a sample are wellbleached the true equivalent dose is provided by thelowest points of the dose distribution provided thatsmall enough aliquots are used (Olley et al 1999reproduced in Fig 6) Alternatively a radial plot can beused for graphical presentation and equivalent dose

Fig 10 Equivalent dose (De) as a function of preheat temperature for six glacigenic quartz samples (redrawn from Rhodes 2000)Measurements were made using a simpli ed version of the SAR procedure (black circles) or using the full SAR procedure (open boxes) Forall samples except GR6 (C) preheating is shown to cause thermal transfer of charge from light-insensitive traps to the OSL traps As a resultequivalent doses will be overestimated when too stringent a preheat is used


determination (Olley et al 1999 reproduced in Fig 7)Obtaining a good estimate is more problematic when alarge percentage of grains are poorly bleached Murrayet al (1995) and Olley et al (1998 1999) demonstratethat the lowest 5 or 10 of the equivalent dosesobtained on small aliquots provide a good estimate ofthe burial dose for their samples Olley et al (1998)report an increase in age with depth for a core of NamoiRiver sediments when the lowest 5 of equivalentdoses is used (Fig 11) However a problem with thismethod is that the result might be erroneously low dueto a normal spread in the results as a consequence ofexperimental errors Lepper et al (2000) propose amore sophisticated method in which the equivalent-dose distribution is deconvoluted to remove scatterresulting from experimental errors the lsquoleading edgersquo ofthe distribution after deconvolution provides the bestestimate of the true equivalent dose (Fig 12)

The above methods use a dose distribution obtainedon a large number of aliquots Fuchs amp Lang (2001)propose a method that can be used for a smaller data setIn this method the equivalent-dose values are orderedfrom lower to higher values and the arithmetic mean iscalculated starting with the two lowermost values andadding additional values until a standard deviation of4 (thought to be the precision of the method) is justexceeded Promising results were obtained for uvial

quartz samples from Greece (Fig 13) but it is clear thatmore aliquots should be used for reliable equivalentdose determination whenever possible especially whenthe sample might be incompletely bleached

It should be pointed out that all these methods rely onthe assumption that at least some of the aliquots containonly grains that had their luminescence signal com-pletely reset prior to deposition If this is not the case

Fig 11 Apparent dose distributions from small aliquots (60ndash100 grains) of 90ndash180 mm quartz from the Namoi River core (Australia redrawnfrom Olley et al 1998) Sampling depths along the core are shown on the right-hand side of each distribution Note that in spite of a widespread in equivalent doses obtained on the aliquots the offset from zero dose of the lowest results at each depth interval increases with sampledepth Using the lowest 5 of the results ages ranging from 22 sect 3 years near the surface to 146 sect 17 years at the base were obtained Theages were found to be generally increasing with depth and consistent with the expected age of the deposit

Fig 12 Noise arising from measurement uncertainties can beremoved by deconvolution the leading edge can be determined afterdeconvolution This is thought to be the true dose for the well-bleached grains in a sample contaminated with poorly bleachedgrains (redrawn from Lepper et al 2000)


the equivalent dose will still be overestimated and theage obtained should be interpreted as a maximum agefor the deposit

Validation of methods

Modern deposits

The offset in age resulting from incomplete zeroing ofthe OSL signal prior to deposition is best assessed bymeasurement of the equivalent dose in samples frommodern deposits Several authors have taken thisapproach in Table 1 an overview is presented of theresults obtained on quartz samples from uvial depositsknown to be less than 500 years old In the Table OSLages are presented based on the mean equivalent dosethe results show a wide spread with offsets from theknown age ranging from 60 to 6500 years

It should be kept in mind that the OSL age based onthe mean equivalent dose will be an overestimate whennot all grains had their luminescence signal completelyreset at the time of deposition The age of a poorlybleached deposit as young uvial deposits can beexpected to be can be more accurately determinedusing the dose distribution obtained on small aliquots orsingle grains of quartz This is clearly demonstrated byOlley et al (1998) who obtained dose distributions onsmall aliquots (60ndash100 grains) from the two lsquomodernrsquosamples shown in Table 1 Using the lowest 5 of thisdose distribution they obtained an OSL age consistentwith zero for the modern sample (ME950022) and an

age of 64 sect 7 years for sample ME95041B which wasdeposited in a ood event 72 years before sampling In afurther study using single quartz grains of the lattersample Olley et al (1999) showed that only 32 of thegrains had measured doses consistent with the expectedburial dose

Values reported by Stokes et al (2001) for largealiquots of quartz from the river bed of the Loire clearlyindicate a decreasing trend of equivalent dose withtransportation distance the highest offsets are foundclose to the source of the river (Fig 14) Murray et al(1995) suggested that overbank deposits are more likelyto be well bleached as they must have been close to thewater surface when the channel ooded However noclear support for this is found in the dataset of Table 1Jain et al (1999) suggest that the modern sample fromthe Luni channel (India) is well-bleached since the localclimatic circumstances cause prolonged dry periodsduring which uvial material is locally reworked bywind

For modern glacio uvial deposits an even widerspread in equivalent doses has been reported (Rhodes ampPownall 1994 Rhodes amp Bailey 1997) This is probablya consequence of the short transport distance of this typeof material (see Gemmell 1997 Stokes et al 2001)Recent investigation has shown that the offset inequivalent dose found for the modern glacio uvialdeposits is largely a consequence of thermal transfer(Rhodes 2000) and can be avoided by using a less-stringent preheat regime

Little information is available for IR-OSL dating offeldspar from modern uvial deposits Porat et al(2001) found a wide range of equivalent doses for uvial samples from a hyper-arid region in IsraelEquivalent doses ranging from 01 Gy up to 30 Gy werereported for individual aliquots Lowest equivalent

Fig 13 In cases where it is not possible or practical to measure theequivalent dose in a large number of aliquots the true equivalentdose might be inferred from an analysis of the single-aliquotequivalent doses on a small number of aliquots (redrawn from Fuchsamp Lang 2001) This graph is a visualization for the procedureexplained in the main text It should be realized that measuring morealiquots of the sample will give more information on the dosedistribution such an approach should therefore be preferredwhenever feasible

Fig 14 Equivalent doses measured for modern bed-load samplescollected in the channel of the River Loire (France redrawn fromStokes et al 2001) For each sample the mean median and minimumequivalent doses obtained on 10 large aliquots are shown A simpleregenerative procedure (cf Murray et al 1995) was applied forequivalent-dose determination and a 10 s 200degC preheat was usedNote the decreasing trend in equivalent doses with increasingdistance downstream


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doses were found for reworked uvial sediments wherethe grains had gone through several cycles of erosionand sedimentation greatest offsets were observed forfreshly eroded bedrock Wallinga et al (2001) report anIR-OSL age of 16 ka for feldspar (180ndash212 mm frac-tion) from the 300-year-old sample from the Rhine-Meuse system discussed in Table 1

Known-age deposits

Murray (1996) determined the age of seven quartzsamples from a sequence of ood deposits on the bankof the Murrumbidgee River at the junction with theTuggeranong Creek New South Wales Australia TheSARA protocol (Mejdahl amp Boslashtter-Jensen 1994) wasused for equivalent-dose determination and age controlwas provided by radiocarbon dating of charcoalincorporated in the deposits at three levels A radio-carbon age of about 2000 years was reported for thebase of the ood deposits whereas charcoal from nearthe top was radiocarbon-dated at about 300 yearsHowever the possibility of reworking of the organicmaterial and hence overestimation of the age ofdeposition cannot completely be ruled out Never-theless the radiocarbon ages and the quartz OSL agesare in good agreement and the OSL ages are in correctstratigraphical order

Olley et al (1999) report quartz OSL ages on a uvialsample from an Australian sediment horizon radio-carbon-dated to a calendar age of 1400ndash1690 yearsMeasurements were made on small aliquots consistingof 60ndash100 grains of quartz The arithmetic meanequivalent dose obtained indicated an age of 24 sect03 ka clearly an overestimation A detailed study ofthe dose distribution of single quartz grains showed thatthe overestimation was caused by contamination with asmall percentage of poorly bleached grains When thelowest 5 of the small-aliquot dose distribution wasused an OSL age in good agreement with the radio-carbon age control was found

Wallinga et al (2001) applied quartz OSL dating to atotal of six samples from four known-age uvialsystems in the Holocene and Late-Weichselian depositsof the Rhine-Meuse system in The Netherlands The ageof the youngest sample was known from historicalmaps whereas the oldest sample contained an abun-dance of pumice from the Laacher See volcaniceruption which has been dated to 132 ka (Friedrich etal 1999) The age of the other two systems wasconstrained by AMS radiocarbon dating of in situorganic material underlying the overbank deposits(indicating the beginning of the activity of the system)and organic material overlying the overbank depositsor lling the residual channel (indicating the end ofactivity of the system) Each aliquot contained about200 grains and the SAR protocol was used forequivalent-dose determination For the youngest samplea slight offset as a consequence of poor bleaching was

found (as discussed in the previous section) For theolder samples excellent agreement was found with theindependently known periods of activity (Fig 15)When the IR-OSL signal of feldspar was used anunderestimation of age was found for the same samples

Straf n et al (1999) and Colls et al (2001) presentquartz OSL ages for ve samples from two known-age uvial terraces of the Loire and Arroux rivers in FranceThe age of the terraces is known from radiocarbondating of wood incorporated in the deposits Goodagreement is reported between quartz OSL datingresults (SAR protocol 10 s preheat at 280degC largealiquots) and radiocarbon ages for two terrace unitswith calibrated radiocarbon ages of 012ndash14 ka and29ndash56 ka respectively Unfortunately the periods offormation of the deposits are fairly long making thecomparison not very stringent Folz et al (2001) tooworked on the Loire and reported a 40 age over-estimation when applying quartz OSL dating to uvialdeposits of known age (sup113 ka) at a Late Paleolithic sitenear Paris Three quartz samples from the site weredated and gave consistent results overestimating theindependent age In spite of a detailed study the reasonsfor the quartz OSL age overestimation could not beidenti ed no indications for poor bleaching werefound

Reports of OSL ages on known-age uvial materialolder than 13 ka are rare Mol et al (2000) present anOSL age of 35 sect 8 ka for quartz from Weichselian uvial deposits of the Spree and Neiszlige rivers in

Fig 15 A comparison of OSL dating results with independent agecontrol (historical and 14C) for a range of samples from Rhine-Meuse uvial deposits in The Netherlands (redrawn from Wallinga et al2001) Using the SAR procedure (10 s 200degC preheat sup1200 grainsper aliquot) OSL ages obtained on the quartz separates were inexcellent agreement with the independent age control Feldspar IR-OSL results obtained by the single-aliquot additive-dose procedure(Duller 1991) gave an age underestimation for the older samples


Germany radiocarbon-dated to 28 ka BP Multiple-aliquot methods were used and the large uncertaintymight be a consequence of incomplete resetting of theOSL signal prior to deposition Tanaka et al (2001)present quartz OSL ages for known-age uvial depositsup to 60 ka in age but their OSL age estimates arescattered and troubled by uncertainties in the watercontent of the material Moreover the independent agecontrol is not presented in their paper which makesassessment of the validity of the comparisons proble-matic

Synthesis

Clearly more research is needed to demonstrate theaccuracy of OSL ages for uvial deposits older thanabout 13 ka For non- uvial deposits accuracy has beenshown by comparison with radiocarbon ages up to 35 kaand by comparison with other techniques up to 300 ka(see review by Murray amp Olley 2002) Promising OSLdating results were also obtained on Eemian (OIS 5e120ndash130 ka) deposits from Denmark (Murray et al2002) Future research should focus on nding possi-bilities for comparison of OSL ages with independentage control to further increase the con dence in quartzOSL dating

The degree of bleaching during uvial transport andthe effect of poor bleaching on luminescence agesobtained remains a topic that deserves attention Seriousage overestimation has been found for deposits wheretransport distances are very short (eg glacial outwash)whereas offsets in downstream stretches of large riversystems are normally small This is likely to be theresult of the numerous cycles of erosion and depositionthe grains go through before being deposited down-stream Also it is possible that the dose in the grainsprior to incorporation in the stream is generally smallerin this environment

OSL dating of young uvial deposits should employsmall aliquots for obtaining information on the dosedistribution in the sample With this information thedegree of bleaching can be determined and accurateOSL age determination is feasible Equipment designedfor the automated measurement of the OSL of singlesand-sized grains is now commercially available(Boslashtter-Jensen et al 2000) and this will greatlyfacilitate single-grain OSL dating More research isneeded if we are fully to understand dose distributionsin single grains (see eg Roberts et al 2000) but it isclear that the possibility of single-grain dating will havea great impact on the luminescence dating of uvialdeposits especially for young sediments Opportunitiesthat are waiting to be explored include the migrationrates of meanders and the rate of alluvial fan aggrada-tion

For older (pre-Holocene) deposits of large riversystems errors arising from incomplete resetting ofthe quartz OSL signal are probably trivial in most cases

Nevertheless caution is always needed and smallaliquots should be used whenever possible A greaterproblem for older deposits might be the onset ofsaturation of the OSL signal of quartz resulting in alesser accuracy and precision for ages greater than100 ka

Some applications

In response to the improvements in the methods andprocedures used for luminescence dating and theresulting leap in the accuracy and reliability of theOSL ages obtained geologists increasingly use OSLdating for obtaining absolute chronologies on uvialdeposits The chronology of many of these depositscould previously not be established due to the lack of asuitable dating method thereby OSL dating enablesnew research questions to be addressed In the followingsection some typical applications that illustrate thepotential of OSL dating in uvial research will bebrie y discussed

Fluvial response to precipitation changes

Srivastava et al (2000) investigated the river adjust-ment and incision in the arid environment of theSabarmati basin (India) From the average age obtainedfrom the OSL dating of quartz and feldspar the authorsconcluded that uvial deposition took place between 54and 30 ka corresponding to a period of less aridity andstronger SW monsoon activity In the period 12 to45 ka the Sabarmati River adjusted its course due totectonism in the region and subsequently incised inresponse to the enhanced SW monsoon and lower sealevel Distinct uplift periods at 3 and 03 ka resulted inpreservation of three lsquoscroll plainsrsquo along the presentriver course

Fluvial response to climate change

Straf n et al (1999) and Colls et al (2001) presentquartz OSL ages for a ight of terraces along the Loireand Arroux Rivers in France (Fig 16) From the datingresults the authors conclude that sediment storageoccurred during lsquoglacialperiglacialrsquo episodes whereasinterglacials are marked by net sediment removal fromthe valley axes Based on a combination of radiocarbonand OSL dating results the transition from a braided tomeandering system could be bracketed between 11 and73 ka Fuller et al (1996 1998) used IR-OSL dating offeldspar to establish the chronology of terracesequences in the Guadalope basin NE Spain An ageof 250 ka was found for the oldest deposits down to04 ka for deposits along the present course of the riverFrom a comparison of the IR-OSL terrace chronologywith high-resolution ice core and marine oxygen isotopeclimate series Fuller et al (1998) conclude that


aggradational episodes coincide with stadial or neo-glacial events while phases of river incision occurduring interstadial or interglacial episodes Unfortu-nately the validity of the IR-OSL ages reported in thiswork is not proven by comparison with independentchronologies Seeing IR-OSL age-underestimationproblems reported elsewhere (eg Lamothe et al1994 Wallinga et al 2001) caution should be takenwhen correlating IR-OSL dated uvial events withclimate proxies

Fluvial response to sea-level changes

Tornqvist et al (2000) report quartz OSL ages onsamples taken from a nearly 50-m-deep core through(predominantly) uvial deposits in the western Nether-lands Using quartz OSL dating uvial deposits fromthe penultimate glacial (Saalian OIS 6) and last glacial(Weichselian OIS 5d - 2) could be identi ed (Fig 17)A combination of the OSL geochronology with litho-logical sedimentological and biostratigraphic analysesallowed the authors to conclude that interglacialcoastal-prism deposits at the sample site were largelyeroded following sea-level fall at the initiation of the

Weichselian glaciation Considerable uvial depositionwas shown to have taken place during later stages ofsea-level fall

Timing of maximum ice-sheet extent

Larsen et al (1999) report quartz OSL ages onglacio uvial deposits in northwest Russia Based onthe ages obtained the authors argue that the maximumextent of the Scandinavian ice sheet was attained about17 ka ago and that deglaciation started close to 15 kaThese ages are younger than those reported for themaximum ice sheet extent farther to the west (Man-gerud et al 2001 2002) and the authors suggest thatinitial ice build-up took place in the west followed by asuccessive migration of the ice divide to the east

Conclusions

Over recent years methods and procedures for OSLdating have improved considerably Using the newestmethods it is possible to accurately determine the ageof uvial sediments deposited during the last glacial

Fig 16 A ight of uvial terraces along the Rivers Loire and Arroux (France) was dated using the OSL signal from large aliquots of sand-sized quartz grains (Straf n et al 1999 Colls et al 2001 the graph is redrawn from those sources) OSL dating of terrace deposits allowedinferences on periods of aggradation and incision to be made (see main text)


cycle The technique now allows ( uvial) geologistsand geomorphologists to explore research questions thatcould not be addressed before

At present the quartz single-aliquot regenerative-dose (SAR) protocol is probably the best method to usefor OSL dating of uvial deposits Measurementsshould be made using small aliquots to improve chancesof detecting poor bleaching and stringent preheatingshould be avoided to evade age overestimation due tothermal-transfer effects Quartz OSL ages reported formodern and young uvial deposits indicate that poor

bleaching can result in an age offset of a few thousandyears when large aliquots are used By detailedinvestigation of the dose distribution using smallaliquots (ideally consisting of a single grain of sand)true ages can be obtained from a poorly bleacheddeposit

Published comparisons of OSL ages and independentage control on uvial deposits are still rare especiallyfor deposits older than 13 ka Most existing compari-sons show good agreement but more proof of thereliability of the method for older deposits is essential toimprove con dence in application of OSL dating todeposits of unknown chronology Recently equipmenthas been developed allowing the automated measure-ment of single sand-sized grains This allows determi-nation of the age of deposits in which not all grains arethoroughly zeroed and is expected to greatly widen theapplicability of OSL dating to uvial deposits espe-cially for young deposits

Acknowledgements ndash This is a contribution to the NEESDI(Netherlands Environmental Earth System Dynamics Initiative)programme I am grateful to Torbjorn Tornqvist (University ofIllinois at Chicago USA) and Ward Koster (Utrecht University TheNetherlands) for commenting on earlier versions of the article Ithank Ann Wintle (University of Wales Aberystwyth UK) andAndrew Murray (Aarhus University Denmark) for their thoroughreviews and many constructive comments on the manuscript I amindebted to Ton Markus (Utrecht University The Netherlands) forredrawing all gures from the original sources Richard BaileyStephen Stokes (both Oxford University) and Andrew Murray arethanked for sending me unpublished manuscripts

ReferencesAitken M J 1998 An Introduction to Optical Dating 267 pp

Oxford University Press New YorkBailey R M 2000 The interpretation of quartz optically stimulated

luminescence equivalent dose versus time plots RadiationMeasurements 32 129ndash140

Bailey R M Smith B W amp Rhodes E J 1997 Partial bleachingand the decay form characteristics of quartz OSL RadiationMeasurements 27 123ndash136

Balescu S amp Lamothe M 1992 The blue emission of K-feldsparcoarse grains and its potential for overcoming TL age under-estimation Quaternary Science Reviews 11 45ndash51

Banerjee D Murray A S Boslashtter-Jensen L amp Lang A 2001Equivalent dose estimation using a single aliquot of polymineral ne grains Radiation Measurements 33 73ndash94

Berger G W amp Luternauer J J 1987 Preliminary eld work forthermoluminescence dating studies at the Fraser River deltaBritish Columbia Geological Survey of Canada Paper 87IA901ndash904

Blum M D amp Tornqvist T E 2000 Fluvial responses to climateand sea-level change a review and look forward Sedimentology47 Supplement 1 2ndash48

Bluszcz A 2001 Simultaneous OSL and TL dating of sedimentsQuaternary Science Reviews 20 761ndash766

Boslashtter-Jensen L Bulur E Duller G A T amp Murray A S 2000Advances in luminescence instrument systems RadiationMeasurements 32 523ndash528

Bulur E 1996 An alternative technique for optically stimulatedluminescence (OSL) experiment Radiation Measurements 26701ndash709

Fig 17 Generalized sedimentary log and a summary of results of aninterdisciplinary investigation of a core through middle to lateQuaternary uvial deposits in the subsurface of the west-centralNetherlands (redrawn from Tornqvist et al 2000) Using acombination of information on shell content (M = marine shellspartly reworked) diatom content (E = estuarine iexcl = no diatoms)pollen content (W = warm C = cool) and dating using the OSL signalfrom sand-sized quartz (mean and two sigma con dence intervalshown) inferences could be made about the timing of uvialdeposition and about the preservation potential of deposits


Clarke M L 1996 IRSL dating of sands bleaching characteristicsat deposition inferred from the use of single aliquots RadiationMeasurements 26 611ndash620

Clarke M L Rendell H M amp Wintle A G 1999 Qualityassurance in luminescence dating Geomorphology 29 173ndash185

Colls A E Stokes S Blum M D amp Straf n E 2001 Age limitson the Late Quaternary evolution of the upper Loire RiverQuaternary Science Reviews 20 743ndash750

Duller G A T 1991 Equivalent dose determination using singlealiquots Nuclear Tracks and Radiation Measurements 18 371ndash378

Duller G A T 1994 Luminescence dating of poorly bleachedsediments from Scotland Quaternary Science Reviews 13 521ndash524

Duller G A T 1996 Recent developments in luminescence datingof Quaternary sediments Progress in Physical Geography 20133ndash151

Folz E Bodu P Bonte P Joron J L Mercier N amp Reyss J L2001 OSL dating of uvial quartz from Le Closeau a LatePaleolithic site near Paris ndash comparison with 14C chronologyQuaternary Science Reviews 20 927ndash933

Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K L1999 Paleo-environment and radiocarbon calibration as derivedfrom LateglacialEarly Holocene tree-ring chronologies Quatern-ary International 61 27ndash39

Fuchs M amp Lang A 2001 OSL dating of coarse-grain uvialquartz using single-aliquot protocols on sediments from NEPeloponnese Greece Quaternary Science Reviews 20 783ndash787

Fuller I C Macklin M G Lewin J Passmore D G amp Wintle AG 1998 River response to high-frequency climate oscillations insouthern Europe over the past 200 ky Geology 26 275ndash278

Fuller I C Macklin M G Passmore D G Brewer P A LewinJ Passmore D G amp Wintle A G 1996 Geochronologies andenvironmental records of Quaternary uvial sequences in theGuadalope basin northeast Spain based on luminescence datingIn Branson J Brown A G amp Gregory K J (eds) GlobalContinental Changes the Context of Palaeohydrology 99ndash120Geological Society Special Publication No 115

Fuller I C Wintle A G amp Duller G A T 1994 Test of the partialbleach methodology as applied to the infra-red stimulatedluminescence of an alluvial sediment from the Danube RadiationMeasurements 23 539ndash544

Galbraith R G 1990 The radial plot graphical assessment ofspread in ages Nuclear Tracks and Radiation Measurements 17207ndash214

Gemmell A M D 1997 Fluctuations in the thermoluminescencesignal of suspended sediment in an alpine glacial meltwaterstream Quaternary Science Reviews 16 281ndash290

Godfrey-Smith D I Huntley D J amp Chen W H 1988 Opticaldating studies of quartz and feldspar sediment extracts Quatern-ary Science Reviews 7 373ndash380

Hansen L Funder S Murray A S amp Mejdahl V 1999Luminescence dating of the last Weichselian Glacier advance inEast Greenland Quaternary Science Reviews 18 179ndash190

Huntley D J amp Berger G W 1995 Scatter in luminescence datafor optical dating ndash some models Ancient TL 13 5ndash9

Huntley D J amp Clague J J 1996 Optical dating of tsunami-laidsands Quaternary Research 46 127ndash140

Huntley D J Godfrey-Smith D I amp Thewalt M L W 1985Optical dating of sediments Nature 313 105ndash107

Huntley D J amp Lamothe M 2001 Ubiquity of anomalous fading inK-feldspars and the measurement and correction for it in opticaldating Canadian Journal of Earth Sciences 38 1093ndash1106

Jain M Tandon S K Bhatt S C Singhvi A K amp Mishra S1999 Alluvial and aeolian sequences along the River LuniBarmer district physical stratigraphy and feasibility of lumines-cence chronology methods Memoir Geological Society of India42 273ndash295

Krause W E Krbetschek M R amp Stolz W 1997 Dating ofQuaternary lake sediments from the Schirmacher Oasis East

Antarctica by infra-red stimulated luminescence IRSL detected atthe wavelength of 560 nm Quaternary Science Reviews 16 387ndash392

Lamothe M amp Auclair M 1999 A solution to anomalous fadingand age shortfalls in optical dating of feldspar minerals Earth andPlanetary Science Letters 171 319ndash323

Lamothe M Balescu S amp Auclair M 1994 Natural IRSL intensitiesand apparent luminescence ages of single feldspar grains extractedfrom partially bleached sediments Radiation Measurements 23555ndash561

Lanesky D E Logan B W Brown R G amp Hine A C 1979 Anew approach to portable vibracoring under water and on landJournal of Sedimentary Petrology 49 654ndash657

Larsen E Lysa A Demidov I Funder S Houmark-Nielsen MKjaer K H amp Murray A S 1999 Age and extent of theScandinavian ice sheet in northwest Russia Boreas 28 115ndash132

Larsen N A Bulur E Boslashtter-Jensen L amp McKeever S W S2000 Use of the LM-OSL technique for the detection of partialbleaching in quartz Radiation Measurements 32 419ndash425

Lepper K Larsen N A amp McKeever S W S 2000 Equivalentdose distribution analysis of Holocene eolian and uvial quartzsands from Central Oklahoma Radiation Measurements 32 603ndash608

Li S-H 1994 Optical dating insuf ciently bleached sedimentsRadiation Measurements 23 563ndash567

Mangerud J Astakhov V I Murray A S amp Svendsen J I 2001The chronology of a large ice-dammed lake and the Barents-KaraIce Sheet advances Northern Russia Global and PlanetaryChange 31 321ndash336

Mangerud J Astakhov V I amp Svendsen J I 2002 The extent ofthe Barents-Kara ice sheet during the Last Glacial MaximumQuaternary Science Reviews 21 111ndash119

Mejdahl V amp Boslashtter-Jensen L 1994 Luminescence dating ofarchaeological materials using a new technique based on singlealiquot measurements Quaternary Science Reviews 13 551ndash554

Mol J Vandenberghe J amp Kasse C 2000 River response tovariations of periglacial climate in mid-latitude Europe Geo-morphology 33 131ndash148

Murray A S 1996 Developments in optically stimulated lumines-cence and photo-transferred thermoluminescence dating of youngsediments application to a 2000-year sequence of ood depositsGeochimica et Cosmochimica Acta 60 565ndash576

Murray A S Marten R Johnston A amp Marten P 1987 Analysisfor naturally occurring radionuclides at environmental concentra-tions by gamma spectrometry Journal of Radioanalytical andNuclear Chemistry 115 263ndash288

Murray A S Olley J M amp Caitcheon G G 1995 Measurementof equivalent doses in quartz from contemporary water-lainsediments using optically stimulated luminescence QuaternaryScience Reviews 14 365ndash371

Murray A S amp Olley J M 1999 Determining sedimentation ratesusing luminescence dating GeoResearch Forum 5 121ndash144

Murray A S amp Olley J M 2002 Precision and accuracy in theoptically stimulated luminescence dating of sedimentary quartz astatus review Geochronometria 21 1ndash15

Murray A S amp Roberts R G 1997 Determining the burial time ofsingle grains of quartz using optically stimulated luminescenceEarth and Planetary Science Letters 152 163ndash180

Murray A S amp Roberts R G 1998 Measurement of the equivalentdose in quartz using a regenerative-dose single-aliquot protocolRadiation Measurements 29 503ndash515

Murray A S amp Wintle A G 2000 Luminescence dating of quartzusing an improved single-aliquot regenerative-dose protocolRadiation Measurements 32 57ndash73

Murray A S Wintle A G amp Wallinga J 2002 Dose estimationusing quartz OSL in the non-linear region of the growth curveRadiation Protection Dosimetry 101 271ndash374

Olley J M Roberts R G amp Murray A S 1997 Disequilibria inthe uranium decay series in sedimentary deposits at Allenrsquos Cave


Nullarbor plain Australia implications for dose rate determina-tions Radiation Measurements 27 433ndash443

Olley J Caitcheon G amp Murray A 1998 The distribution ofapparent dose as determined by optically stimulated luminescencein small aliquots of uvial quartz implications for dating youngsediments Quaternary Science Reviews 17 1033ndash1040

Olley J M Caitcheon G G amp Roberts R G 1999 The origin ofdose distributions in uvial sediments and the prospect of datingsingle grains from uvial deposits using optically stimulatedluminescence Radiation Measurements 30 207ndash217

Poolton N R J Ozanyan K B Wallinga J Murray A S ampBoslashtter-Jensen L 2002 Electrons in feldspar II a consideration ofthe in uence of conduction band-tail states on luminescenceprocesses Physics and Chemistry of Minerals 29 217ndash225

Porat N Zilberman E Amit R amp Enzel Y 2001 Residual ages ofmodern sediments in an hyperarid region Israel QuaternaryScience Reviews 20 795ndash798

Prescott J R amp Hutton J T 1994 Cosmic ray contributions to doserates for luminescence and ESR dating large depths and long-termtime variations Radiation Measurements 23 497ndash500

Preusser F 1999a Luminescence dating of uvial sediments andoverbank deposits from Gossau Switzerland ne grain datingQuaternary Science Reviews 18 217ndash222

Preusser F 1999b Bleaching characteristics of some opticallystimulated luminescence signals Ancient TL 17 11ndash14

Rhodes E J 1990 Optical dating of quartz from sediments PhDdissertation Oxford University 153 pp

Rhodes E J 2000 Observations of thermal transfer OSL signals inglacigenic quartz Radiation Measurements 32 595ndash602

Rhodes E J amp Bailey R M 1997 The effect of thermal transfer onthe zeroing of the luminescence of quartz from recent glacio uvialsediments Quaternary Science Reviews 16 291ndash298

Rhodes E J amp Pownall L 1994 Zeroing of the OSL signal in quartzfrom young glacio uvial sediments Radiation Measurements 23581ndash585

Richardson C A 2000 Preheat-induced signal enhancement in theinfrared stimulated luminescence of young and bleached sedimentsamples Radiation Measurements 32 541ndash547

Roberts H M amp Wintle A G 2001 Equivalent dose determina-tions for polymineralic ne-grains using the SAR protocolapplication to a Holocene sequence of the Chinese Loess PlateauQuaternary Science Reviews 20 859ndash863

Roberts R G Spooner N A amp Questiaux D G 1994a Palaeodoseunderestimates caused by extended duration preheats in the opticaldating of quartz Radiation Measurements 23 647ndash653

Roberts R G Jones R Spooner N A Head M A Murray A Samp Smith M A 1994b The human colonisation of Australiaoptical dates of 53000 and 60000 years bracket human arrival atDeaf Adder gorge Northern Territory Quaternary ScienceReviews 13 575ndash584

Roberts R G Galbraith R F Yoshida H Laslett G M amp OlleyJ M 2000 Distinguishing dose populations in sediment mixturesa test of single-grain optical dating procedures using mixtures oflaboratory-dosed quartz Radiation Measurements 32 459ndash465

Smith B W amp Rhodes E J 1994 Charge movements in quartz andtheir relevance to optical dating Radiation Measurements 23329ndash334

Smith D G 1984 Vibracoring uvial and deltaic sediments tips onimproving penetration and recovery Journal of SedimentaryPetrology 54 660ndash663

Sowers J M Noller J S amp Lettis W R 2000 Methods for datingQuaternary sur cial materials In Noller J S Sowers J M ampLettis W R (eds) Quaternary Geochronology Methods andApplications 582 pp American Geophysical Union ReferenceShelf Series 4 Washington DC

Spooner N A 1993 The Validity of Optical Dating Based onFeldspar 207 pp PhD dissertation Oxford University

Spooner N A 1994a On the optical dating signal from quartzRadiation Measurements 23 593ndash600

Spooner N A 1994b The anomalous fading of infrared-stimulated

luminescence from feldspars Radiation Measurements 23 625ndash632

Srivastava P Juyal N Singhvi A K Wasson R J amp BatemanM D 2001 Luminescence chronology of river adjustment andincision of Quaternary sediments in the alluvial plain of theSabarmati River north Gujarat India Geomorphology 36 217ndash229

Stokes S 1994 Optical Dating of Selected Late Quaternary AeolianSediments from the Southwestern United States PhD disserta-tion Oxford University 593 pp

Stokes S 1999 Luminescence dating applications in geomorpho-logical research Geomorphology 29 153ndash171

Stokes S amp Walling D In press Chemical and physical methodsfor the direct dating and tracing of uvial sediments In Piegay Hamp Kondolf M (eds) Tools in Fluvial Geomorphology AHandbook for Geologists Hydrologists Engineers Biologistsand Planners Wiley amp Sons Chichester

Stokes S Bray H E amp Blum M D 2001 Optical resetting in largedrainage basins tests of zeroing assumptions using single-aliquotprocedures Quaternary Science Reviews 20 879ndash885

Straf n E C Blum M D Colls A amp Stokes S 1999 Alluvialstratigraphy of the Loire and Arroux Rivers Quaternaire 10 271ndash282

Tanaka K Hataya R Spooner N A amp Questiaux D G 2001Optical dating of river terrace sediments from Kanto plains JapanQuaternary Science Reviews 20 825ndash828

Tornqvist T E Wallinga J Murray A S de Wolf HCleveringa P amp de Gans W 2000 Response of the Rhine-Meuse system (west-central Netherlands) to the last Quaternaryglacio-eustatic cycles a rst assessment Global and PlanetaryChange 27 89ndash111

Vandenberghe J amp Maddy D 2000 The signi cance of uvialarchives in geomorphology Geomorphology 33 127ndash130

Wallinga J 2002 Detection of OSL age overestimation usingsingle-aliquot techniques Geochronometria 21 17ndash20

Wallinga J Duller G A T Murray A S amp Tornqvist T E 2001Testing optically stimulated luminescence dating of sand-sizedquartz and feldspar Earth and Planetary Science Letters 193617ndash630

Wallinga J Murray A S amp Duller G A T 2000 Underestimationof equivalent dose in single-aliquot optical dating of feldsparscaused by preheating Radiation Measurements 32 691ndash695

Wallinga J amp Van der Staay J 1999 Sampling in waterloggedsands with a simple hand-operated corer Ancient TL 17 59ndash61

Wintle A G 1973 Anomalous fading of thermoluminescence inmineral samples Nature 245 143ndash144

Wintle A G 1997 Luminescence dating laboratory procedures andprotocols Radiation Measurements 27 769ndash817

Wintle A G amp Murray A S 2000 Quartz OSL effects of thermaltreatment and their relevance to laboratory dating proceduresRadiation Measurements 32 387ndash400

Appendix A practical guide to sampling uvial deposits for OSL datingIdeally sampling for luminescence dating should be carried out withboth the geologistgeomorphologist and the dating specialist presentUnfortunately this is not always possible and therefore somepractical guidelines are presented below for geologists wanting totake samples from uvial deposits for OSL dating

Location Samples should be taken from a relatively homogeneouslayer at least 20ndash30 cm from boundaries and large lithologicalchanges Giving the reservations about poor bleaching and otherpossible inaccuracies it is advisable to take at least two preferablythree samples from a single sedimentary unit A single OSL date perunit is likely to raise more questions than it will answer unlessseveral layers in a good stratigraphic sequence are successfully dated

Equivalent-dose sample The equivalent dose can be estimated


using either silt (4ndash11 mm) or sand-sized (90ndash425 mm) materialCoarser grains are not suitable because of incomplete penetration ofthe beta dose used for equivalent-dose determination Measurementsare normally made on a relatively narrow grain-size range (eg 90ndash125 or 180ndash250 mm) and the amount of sample that needs to be takenis dependent on the lithology of the material One kilogram ofmaterial normally suf ces but in some cases more is needed (egwhen sand-sized grains from a ne-grain matrix are to be analysed)The sample for the equivalent-dose determination should not beexposed to light at any point during sampling or sample preparationIn an unconsolidated exposure this can be achieved by pushing orhammering an opaque PVC or metal tube into the wall immediatelyclosing both ends after taking the sample It is important that the tubeis completely full to avoid mixing during transport and to allowdisposal of the light-exposed outer parts in laboratory safelightconditions Consolidated material can be sampled by cutting a blockfrom the material and removing the light-exposed outer parts in thelaboratory In case an exposure is not available samples can also betaken using a simple hand-operated corer (Wallinga amp Van der Staay1999) or more sophisticated drilling systems such as the vibrocore(Lanesky et al 1979 Smith 1984)

Annual dose sample Measurements for the dose rate can be madein the eld using a portable gamma-spectrometer Such measure-ments are essential whenever there is doubt about the uniformity ofradioactivity in a 20ndash30 cm layer around the equivalent-dose sampleand require the presence of a specialist Alternatively samples for theannual-dose determination can be taken from around the sampletaken for equivalent-dose determination High-resolution gamma-ray

spectroscopy (Murray et al 1987) can be used to measure the activityof several individual radionuclides in the thorium and uranium decaychains The dose rate can then be evaluated and checks can be maderegarding the equilibrium of the decay chains Alternatively the doserate can be calculated from the concentration of radionuclidesmeasured using for example neutron activation analysis X-ray uorescence or ICP-MS It is important that the sample is thoroughlyhomogenized prior to taking the small subsample used fordetermining the radionuclide concentration Checks on the equili-brium of decay chains can be made by thick-source alpha-countingAdvantages and disadvantages of the techniques are discussed byAitken (1998 pp 46ndash47)

The water content of the deposit during its geological history isimportant as water absorbs radiation thereby diminishing the annualdose The in situ water content is determined by weighing the samplebefore and after drying in OSL dating the water content is normallyexpressed as the weight of the water (ie weight loss on drying)divided by the weight of the dry sample Uncertainties in the watercontent estimate will result in errors on the age obtained with a 1error in water content roughly resulting in 1 error in age

Finally the depth of the deposit below the surface andinformation on its burial history as well as the geomagneticlatitude of the sample position are needed to allow estimation of thecosmic dose (for details see Aitken 1998 Prescott amp Hutton 1994)In northern Europe the relative contribution of cosmic rays to thetotal dose is normally small thereby making the OSL age lesssensitive to assumptions made with regard to changes in overburdensince burial


ologies for uvial deposits The paper is addressed tothe user community wishing to use OSL dating tech-niques to establish the chronology of ( uvial) depositsas well as to the OSL dating community The paperdescribes and discusses the methods and proceduresused for OSL dating Much attention is given to thedetection of incomplete resetting of the luminescencesignal prior to deposition because of its relevance to theOSL dating of uvial deposits The validity of the OSLages is discussed by reviewing OSL dating results on uvial deposits of known chronology many of whichare modern Finally examples are discussed of geo-logical applications of OSL dating to uvial deposits ofunknown chronology

Luminescence dating

After sedimentation grains of quartz and feldspar areburied and exposed to low-level ionizing radiationwhich is produced by the decay of naturally occurringradionuclides (mainly of the U and Th series and 40K)and a in most cases relatively small contribution fromcosmic rays During this exposure to ionizing radiationfree charge carriers (electrons and holes) are producedand some of them are trapped at defects in the crystallattice (Fig 1) Charge trapped in the OSL traps is stableover long periods of time but is released when themineral is exposed to light Hence the total amount ofcharge in these traps will increase with burial time but

the charge is released when the mineral grains areeroded and transported in daylight Thus the amount oftrapped charge forms a clock that starts ticking from themoment the mineral is buried and shielded from light

Luminescence dating makes use of the physicalphenomenon of luminescence a very small light uxresulting from the recombination of electrons releasedfrom traps and holes Recombination can be forcedeither by heating the mineral (TL) or by exposing it tolight (OSL) The brightness of the luminescence signalre ects the amount of charge trapped and hence theirradiation dose the sample has received since burial(equivalent dose) The age of a sample is given by thefollowing equation where the annual dose is theirradiation dose ux in the natural environment

Age(a) ˆ equivalent dose (Gy)annual dose (Gya)

Luminescence dating allows determination of abso-lute ages in the range of years to one million years Atthe lower end of the age range the technique is limitedby incomplete resetting of the OSL signal prior todeposition this will be discussed in detail in the nextsection The maximum age for application of OSLdating is determined by saturation of the traps in thecrystal For quartz this usually limits its application tothe last 150 ka whereas for feldspar dating up to 1 Ma ispossible in principal The precision of age estimationsfor sediments with low luminescence sensitivity can belimited by the dimness of the luminescence signal thisapplies especially in the case of young deposits

A wide range of measurement procedures is used forequivalent-dose determination of both quartz andfeldspar separates In this section the general termsare explained Wintle (1997) Aitken (1998) andMurray amp Wintle (2000) provide a full accountEquivalent-dose determination involves establishinghow much radiation exposure is needed to obtain anOSL signal identical to that resulting from naturalradiation exposure

In traditional methods (the multiple-aliquot proce-dures) a number of aliquots (subsamples each contain-ing a few hundred to a few thousand grains 2ndash15 mg ofmaterial) are prepared and divided into groups eachcontaining at least three aliquots One group is used formeasurement of the natural OSL signal The othergroups are given various doses either on top of theirnatural dose (for additive-dose procedures) or afterexposure to light (for regenerative-dose procedures) Adose-response curve is constructed from measurementson each group and the equivalent dose is obtained byextrapolation of this curve (in additive-dose proce-dures) or by projection of the natural OSL signal on thiscurve (in regenerative-dose procedures) (Fig 2) Dis-advantages of multiple-aliquot procedures are thatnormalization is needed to account for aliquot-to-aliquot differences in luminescence sensitivity and

Fig 1 Simpli ed energy-level diagram showing the electron andhole transitions that are responsible for the occurrence of OSL(redrawn from Aitken 1998 p 14) A At exposure of the crystal toradiation ionization results in the trapping of electrons and holes atdefects T and L respectively B To be used for dating the lifetime ofthe electrons in the traps needs to be at least several million yearsThis is the case for traps giving rise to the quartz OSL signal CExposure to light of the appropriate wavelength will evict electronsfrom traps Subsequent recombination with holes trapped atluminescence centres will give rise to the emission of a minute lightemission called optically stimulated luminescence














































What method to use








Grain size



Preheat
























Modern deposits










Tab

le1

An

over

view

ofqu

artz

OS

Lda

ting

resu

ltson

sam

ples

youn

ger

than

500

year

s

Aut

hor

Sam

ple

Dep

osit

De

(mea

nse

)M

etho

dP

rehe

atG

rain

size

( mm

)A

liqu

otsi

ze(g

rain

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OS

Lag

e(y

ears

)(m

ean

se)

Exp

ecte

dag

e(y

ears

)

Col

lset

al(

2001

)L

oire

Riv

er1

91

Poin

tbar

19

sect0

3S

AR

10s

280deg

C90

ndash212

sup135

00c1

635

0sect

70lsquom

oder

nrsquoL

oire

Riv

er1

91

Poin

tbar

14

sect0

3S

AR

10s

280deg

C42

5ndash60

0sup1

300c1

630

0sect

60lsquom

oder

nrsquoJa

inet

al(

1999

)97

-TR

-131

Riv

erB

ed0

16sect

004

MA

AD

5m22

0degC

105ndash

150

ndashndash

ndashlsquom

oder

nrsquoM

urra

yet

al(

1995

)M

urra

y(1

996)

Tug

Cre

ek9

3800

7O

verb

ank

040

sect0

04S

AR

A10

s19

0degC

90ndash2

50sup1

1800

c23

100

sect13

5ndash30

0

Mur

ray

(199

6)93

8001

Ove

rban

k1

07sect

005

SA

RA

10s

190deg

C10

6ndash21

2sup1

1500

c26

300

sect25

190ndash

440

Mur

ray

etal

(19

95)

Beg

aR

iver

Est

uary

Ove

rban

k0

21sect

004

SA

RA

10s

200deg

C90

ndash250

sup115

0c212

0ndashd

lt10

Mur

rum

bige

eR

iver

atH

ayC

hann

el1

05sect

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RA

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200deg

C90

ndash250

sup115

0c212

0ndashd

lt30

Bar

won

Riv

erat

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gett

Cha

nnel

37

sect0

5S

AR

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s20

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tail

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Age

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tain

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ian

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Gy

kado

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te(b

ased

onC

olls

etal

20

01)



Known-age deposits










Synthesis






Some applications













Conclusions
























































































































































What method to use








Grain size



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Tab

le1

An

over

view

ofqu

artz

OS

Lda

ting

resu

ltson

sam

ples

youn

ger

than

500

year

s

Aut

hor

Sam

ple

Dep

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De

(mea

nse

)M

etho

dP

rehe

atG

rain

size

( mm

)A

liqu

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ze(g

rain

s)na

OS

Lag

e(y

ears

)(m

ean

se)

Exp

ecte

dag

e(y

ears

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Col

lset

al(

2001

)L

oire

Riv

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6)93

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Ove

rban

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RA

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190deg

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1500

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300

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95)

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aR

iver

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rban

k0

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RA

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200deg

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rum

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won

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over

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year

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ribu

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best

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tail

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Age

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tain

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med

ian

equi

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sean

das

sum

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a3

Gy

kado

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te(b

ased

onC

olls

etal

20

01)



Known-age deposits










Synthesis






Some applications













Conclusions







































































































































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Grain size



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Modern deposits










Tab

le1

An

over

view

ofqu

artz

OS

Lda

ting

resu

ltson

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ples

youn

ger

than

500

year

s

Aut

hor

Sam

ple

Dep

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De

(mea

nse

)M

etho

dP

rehe

atG

rain

size

( mm

)A

liqu

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ze(g

rain

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OS

Lag

e(y

ears

)(m

ean

se)

Exp

ecte

dag

e(y

ears

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Col

lset

al(

2001

)L

oire

Riv

er1

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Poin

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6)93

8001

Ove

rban

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RA

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190deg

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1500

c26

300

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440

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95)

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aR

iver

Est

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Ove

rban

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200deg

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Mur

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bige

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200deg

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won

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98)

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ased

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01)



Known-age deposits










Synthesis






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Conclusions


























































































































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le1

An

over

view

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artz

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ting

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ltson

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ger

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year

s

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hor

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2001

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ased

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01)



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le1

An

over

view

ofqu

artz

OS

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ting

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ltson

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ger

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year

s

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hor

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ple

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etho

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ears

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dag

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ears

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2001

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95)

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view

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Known-age deposits










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Conclusions






















































































































Synthesis






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Conclusions



























































































































Conclusions





























































































































































































































































































































































































Date post:	10-Nov-2023
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Optically stimulated luminescence dating of fluvial deposits: a review

Documents