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Discontinuous late Pleistocene‐Holocene pollenrecords from Auckland Domain, northern NewZealandMark Horrocks a b , Andy O'Loan c & Rod Wallace da Microfossil Research Ltd , 31 Mont Le Grand Rd, Mt Eden, Auckland, 1024,New Zealand E-mail:b School of Geography, Geology and Environmental Science , University ofAuckland , Private Bag 92019, Auckland, 1142, New Zealandc 1 Tamahere Drive Glenfield, Auckland, 0629, New Zealandd Department of Anthropology , University of Auckland , Private Bag 92019,Auckland, 1142, New ZealandPublished online: 18 Feb 2010.

To cite this article: Mark Horrocks , Andy O'Loan & Rod Wallace (2009) Discontinuous late Pleistocene‐Holocenepollen records from Auckland Domain, northern New Zealand, New Zealand Journal of Botany, 47:3, 239-247,DOI: 10.1080/00288250909509807

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New Zealand Journal of Botany, 2009, Vol. 47: 239-247 2391175-8643 (Online); 0028-825X (Print)/09/4703-0239 © The Royal Society of New Zealand 2009

Discontinuous late Pleistocene-Holocene pollen recordsfrom Auckland Domain, northern New Zealand

MARkHORROckSMicrofossil Research Ltd31 Mont Le Grand RdMt Eden, Auckland 1024, New Zealandemail: info@microfossilresearch.com

andSchool of GeographyGeology and Environmental ScienceUniversity of AucklandPrivate Bag 92019,Auckland 1142, New Zealand

ANDy O'LOAN1 Tamahere DriveGlenfield, Auckland 0629, New Zealand

ROD WALLAcEDepartment of AnthropologyUniversity of AucklandPrivate Bag 92019,Auckland 1142, New Zealand

Abstract Two sediment sequences from Pukekawacrater, Auckland Domain, contain silty clay under-lain by fibrous peat. The peat contains a pollen floraand wood indicating the presence of a warm-tem-perate, conifer-hardwood forest with Metrosideros,Agathis, Prumnopitys taxifolia, P. ferruginea, andespecially Dacrydium. Radiocarbon dates indicatethat the peat was deposited before the Last GlacialMaximum (LGM). Absence of tephras and smallamounts of Fuscospora pollen indicate probablenon-preservation of the LGM. The pollen flora ofmost of the clay contains Metrosideros, Ascarina,and ferns, indicating post-LGM warmer, wetter con-ditions. The two uppermost samples contain exoticpollen, indicating that they are post-European inorigin. Excavation and levelling to form sports fields

B09014; Online publication date 3 September 2009Received 21 May 2009; accepted 6 July 2009

and parkland appears to have curtailed and mixedthe Holocene record.

Keywords Late Pleistocene; Holocene; pollen;vegetation; climate change; Auckland Isthmus;New Zealand

INTRODUCTION

Most of the late Pleistocene-Holocene pollen recordsfrom central Auckland are associated with the Auck-land Volcanic Field, which comprises numerous(c. 50) small volcanoes (Searle 1981; kermode1992). These extinct basaltic maars or scoria cones,or a combination of both, erupted during the Pleis-tocene-Holocene. Several of the maar craters, Pu-kaki crater (Dickinson 2001; Sandiford et al. 2001,2003), Onepoto Basin (Shane & Sandiford 2003),Lake Pupuke (Horrocks et al. 2005a), kohuora crater(Newnham et al. 2007), and the maars associatedwith the scoria cones of crater Hill (Lancashire etal. 2002), Mt Richmond (Sandiford et al. 2002), andMcLaughlins Mountain (Horrocks et al. 2007b),have recently been analysed for fossil pollen andtephra to provide vegetation histories (Fig. 1). Someof the Auckland volcanics also caused the formationof adjacent wetlands by damming waterways withlava. One of these wetlands, Waiatarua (Newnham &Lowe 1991 ; Horrocks et al. 2002), has similarly beenstudied. In addition, pollen preserved in the baseof the scoria cone crater at Mt St John (Fig. 1) hasbeen analysed (Horrocks et al. 2005b). collectively,these studies describe a late Pleistocene-Holoceneenvironmental record of central Auckland coveringthe last 76 000 yr, which is summarised below (fromHorrocks et al. 2007b).

The central Auckland vegetation at c. 76 000 yrBP comprised conifer-hardwood forest with someFuscospora. Dominant taxa were Dacrydium cu-pressinum and Prumnopitys taxifolia accompaniedby Metrosideros. During 64 400-60 500 yr BP (cor-responding to the thermal minima of marine isotopestage 4), there appears to have been an opening of

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-36° 50'S

174°40'E

PukekawaCrater*

Mt St John^ Waiatarua^-A • 7

Fig. 1 Auckland region showingsites mentioned in text ( • volcaniccone).

the canopy, with Coprosma and Halocarpus expand-ing. The 60 500-50 500 yr BP period, interpretedas warming at the start of marine isotope stage 3,shows a rapid expansion of conifer-hardwood for-est still dominated by D. cupressinum and P. taxi-folia, with little Fuscospora, and eventual declineof D. cupressinum. Fuscospora forest expandedrapidly c. 50 000 yr BP and remained dominantuntil c. 23 000 yr BP, suggesting a thermal decline.From c. 23 000-16 500 yr BP, continued coolingrestricted forest to patches within extensive shrub-land/grassland. After this period, conifer-hardwoodforest dominated by P. taxifolia became the mainvegetation cover. After 10 000 yr BP, D. cupressi-num became dominant and taxa indicative of moist,mild, relatively frost-free climates, such as Ascarina

lucida and Metrosideros, expanded. Subsequently,Agathis australis, Libocedrus, and Phyllocladusexpanded after c. 7000 yr BP (but not at every site),suggesting a change to drier conditions. One of thesites covering the last millennium, Lake Pupuke,provides a reliable date for large-scale Polynesiandeforestation shortly before deposition of the c. 700yr BP Rangitoto tephra, erupted from an adjacentvolcano (Horrocks et al. 2005a).

Presented here are results of a pollen investigationof another Auckland maar, Pukekawa volcano, at theAuckland Domain on the Auckland isthmus (Fig. 1).A proposed upgrade of the playing field presentedthe opportunity to examine auger profiles for fossilpollen analysis to provide records of past vegetationand environments (Horrocks 2009).

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Horrocks et al.—Pollen records from Auckland Domain 241

Fig. 2 Pukekawa crater, Auck-land Domain, showing auger sitelocations (contours in metres abovesea level).

THE STUDY AREA

Pukekawa is a Pleistocene volcano situated at Auck-land Domain (a public reserve) on the Aucklandisthmus, the central residential area of Auckland city(Fig. 1). The timing of the eruption is uncertain. Thesummit is c. 80 m above sea level, the crater rim isup to c. 450 m wide, and the catchment is confinedto the crater itself (Fig. 2). The base of the crateris c. 60 m above sea level and is mostly flat exceptfor a small scoria cone (Pukekaroa) in the centre.The crater is surrounded by a horseshoe ring oftuff, created by at least one major explosion (Searle1981). At least one small lava flow also issued fromthe crater.

Auckland has a warm-temperate to subtropicalclimate; mean annual air temperature at AucklandDomain is 15.5-16.0°c (Hessel 1988). Mean annualrainfall is 1000-1200 mm, with a winter maximum.At adjacent Albert Park ( 1 km north-west), the aver-age number of days of ground frost is c. 4.

Pre-historic occupation of Auckland Domain isevident in the presence of pits, terraces, and shellmiddens. Foster (2003) considered that an area suchas the domain would be expected to have more ofthese features, and concluded that further unre-corded sites will likely be present, especially in

areas currently covered in bush. The domain hasbeen extensively modified in European times (Searle1981; Foster 2003). In particular, construction ofa cricket field in the 1860s involved draining andlevelling of the former crater wetland. Duck ponds inthe domain are fresh water fed by these early drains.Further impacts include construction of buildings in1913 for an industrial and mining exhibition.

METHODS

In April 2008, two hand auger profiles from Puke-kawa crater at Auckland Domain were sampled forfossil pollen analysis. One of the auger sites (HA1)is near the southern extremity of the crater and theother (HA6) 420 m to the north near the duck ponds(Fig. 2). Sampling depths were 65-585 cm and 200-545 cm for HA1 and HA6, respectively.

The samples were prepared for pollen analysisby the standard acetylation method (Moore et al.1991). The pollen sum was at least 250, excludingLeptospermum type, wetland taxa, and ferns andallies except Pteridium, which may form extensivedryland stands. These are excluded because they aremostly local taxa tending to have fluctuating pollenand spore production which may distort percentages.

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They are still expressed as a percentage of the basecount, therefore the total of the pollen and sporevalues of each sample in the pollen diagrams mayexceed 100%. Microscopic fragments of charcoalwere extracted, along with pollen, during prepara-tion; presence/absence in each sample was noted.Zone boundaries were defined subjectively and re-flect major changes in pollen assemblages.

Three accelerator mass spectrometry (AMS) ra-diocarbon age determinations (two on HA1 and oneon HA6) were carried out by the Radiocarbon DatingLaboratory, University of Waikato (Table 1).

RESULTS

HA1

The HA1 domain profile comprises fibrous peat withminor sandy silt at c. 585-185 cm depth, silty clayat c. 185—80 cm depth, and silty sand at c. 80-0 cmdepth (Fig. 3). As the auger hole was terminated at600 cm, peat deposits continue to an unknown depthin the crater at this particular site.

Zone 1, 585-200 cm: The pollen sum of Zone 1 isdominated by tall tree taxa: Agathis, undifferen-tiated podocarps, and especially Dacrydium andMetrosideros (Fig. 3). Macrofossil wood of Met-rosideros was found at depths of 525, 325, and230 cm. Wood of another, unidentified angiospermwas found at 325 cm depth. Prumnopitys taxifoliaand P.ferruginea make up most of the undifferenti-ated podocarp pollen ("undif. podocarps"). Pollenof several other tall trees, notably Dacrycarpus,Libocedrus, Nestegis, and Podocarpus, is recordedin small amounts.

Shrubs and small trees are represented mostly byLeptospermum type, which records some very highvalues throughout this part of the profile. Pollen ofother small trees and shrubs, notably Coprosma andMyrsine, is recorded in small amounts. Elaeocarpuspollen increases near the upper zone boundary.

Pollen of the wetland plant community is dom-inated by Myriophyllum and cyperaceae. Small

amounts of other wetland taxa, notably Botryococcus(an alga) and Potamogeton, are also recorded. Herbsand ferns (except for small amounts of Cyatheatree ferns and monolete fern taxa) record very lowvalues.

Zone 2,200-90 cm: A radiocarbon age determinationfrom near the bottom of this zone (at 205 cm depth)yielded a date of 43 639 ± 1490 yr 1 4 c BP (Table1). The zone is characterised by a decline, oftensudden, in pollen of many taxa, namely Agathis,Libocedrus, Metrosideros, Coprosma, Elaeocarpus,Leptospermum type, Botryococcus, Potamogeton,and cyperaceae (Fig. 3). There are coincident peaksin pollen of Fuscospora trees and Ericaceae andMyrsine shrubs, while Poaceae pollen shows a smallsustained increase. There is also an increase in pol-len and spores of several taxa near the upper zoneboundary, namely Metrosideros and Laurelia trees,shrubs and small trees of Ascarina and Hebe, andCyathea and monolete fern taxa. Podocarp wood,identified as possibly Dacrydium, was found atdepths of 195 and 165 cm. Microscopic fragmentsof charcoal first appear in this zone, initially brieflymid-zone (at 155-145 cm depth), then again near thetop of the zone (at 105 cm depth) and continue forthe remainder of the profile. Another radiocarbon agedetermination, from the sample immediately belowthe start of the upper charcoal layer (at 115 cm depth)yielded a date of 7332 ± 30 yr 1 4 c BP (Table 1).

Zone 3, 90-65 cm: Zone 3 is characterised by thefirst appearance of Pteridium and Anthocerotaespores and Taraxacum type and Pinus pollen (Fig. 3).Knightia and Freycinetia pollen also increase. In ad-dition, Poaceae pollen shows a further increase.

HA6

The HA6 domain profile comprises fibrous peatwith minor sandy silt at c. 545-375 cm depth,clayey silt at c. 375-280 cm depth, silty clay at280-220 cm depth, silt at 220–40 cm depth, andsilty sand at 40-0 cm depth (Fig. 4). The peat wasunderlain by medium to coarse sand, and the au-gering was terminated at 585 cm depth on a rocky

Table 1

Profile(HA)

116

AMS radiocarbon data from Auckland Domain. *Mccormac et al. 2004;

Laboratory no.(Wk-)

253332334523346

depth(cm)

115205385

Fraction

silty claypeatpeat

1 4 c(yrBP)

7332 ± 3043639 ±1490

>47000

f beyond calibration curve.

cal. yrBP*(95.4% prob.)

8095 ± 85

tt

δ 1 3 c±2.0

-26.7-27.6

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Shrubs & small tree!

Fig. 3 Pollen percentagediagramofprofileHAl fromPukekawa crater, AucklandDomain.

100 200 300 400

I5"

aen

Io

siltysand siltyclay fibrous peat w. minorsandysilt

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244 New Zealand Journal of Botany, 2009, Vol. 47

obstruction. Samples above 365 cm depth did notcontain sufficient pollen for analysis. However,exotic (Pinus) pollen was found at 280 cm depth,indicating modern disturbance of the profile to atleast this depth.

Zone 1, 545-520 cm: The pollen sum of Zone 1 ischaracterised by Dacrydium and other podocarps

and especially Metrosideros (Fig. 4). Wetland taxa,notably Myriophyllum and cyperaceae, record highpollen values, as do monolete fern taxa.

Zone 2, 520-405 cm: This zone corresponds withZone 1 of the HA1 profile, where Metrosideros andpodocarps dominate the pollen sum and Leptosper-mum type pollen also shows high values (Fig. 4).

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Horrocks et al.—Pollen records from Auckland Domain 245

Other similarities include a peak in Elaeocarpuspollen, substantial Myriophyllum and sedge pol-len, and generally low fern spore values. A majordifference is a broad peak in Dacrycarpus polleninHA6.

Zone 3,405-365 cm: Zone 3 corresponds with Zone2 of the HA1 profile, with slight increases in Hebeand Myrsine pollen and fern spores and decreases inLeptospermum type and cyperaceae pollen (Fig. 4).Macrofossil wood of Metrosideros was found at375 cm depth. Charcoal was not found in this profile.A radiocarbon age determination from near the top ofthe peat (at 385 cm depth) yielded a date of >47 000yr 14c BP (Table 1).

DISCUSSION AND CONCLUSIONS

The two radiocarbon dates from near the top ofthe peaty deposits of each Pukekawa crater pro-file, at the limits of radiocarbon dating, provideminimum ages of c. 45 000 yr BP for those sectionsof the profiles (Table 1, Fig. 3, 4). Although thereis silty sand slopewash in the peat, it is minor, sopossible reworked, older carbon (eroded from thecrater walls) within the dated deposits is probablynot of major significance. On the other hand, thereis the possibility of contamination with youngercarbon, which would mean that the deposit in theHA1 profile with the date of 43 639 ± 1490 yr 14cBP is older than this.

The crater record from Auckland Domain com-mences at an undetermined time before 47 000 yrBP (Table 1). A minimum age for the eruption ofPukekawa at the domain is provided by the wide-spread distal Rotoehu tephra, which erupted fromthe Okataina Volcanic centre in the central NorthIsland some time between c. 45 000 and 65 000 yrBP (Shane & Sandiford 2003). Although not found ineither of the two auger profiles, this tephra has beenidentified in deposits from elsewhere in Pukekawacrater (Phil Shane pers. comm.).

Pollen preserved in the peat section of the HA1profile indicates that before c. 43 500 yr BP, this partof the Pukekawa crater floor environment compriseda Leptospermum-cyperaceae-dominated wetland,probably fringed by Coprosma shrubs (Fig. 3). Thepresence of the aquatic plants Botryococcus, Pota-mogeton, and Myriophyllum indicate frequent inun-dation and open surface water at the site. Vegetationon the dry, crater slopes surrounding the wetland(and in the region) comprised tall, dense conifer-hardwood forest, with the canopy dominated by

Metrosideros. Emerging through this canopy wereconifers, notably Agathis and several podocarps, thelatter including Prumnopitys taxifolia, P.ferruginea,and especially Dacrydium. The pollen category"undif. podocarps" includes mostly P. taxifolia andP.ferruginea.

At the start of the peat sequence of the HA6profile (>47 000 yr BP), cyperaceae and monoletefern taxa appear to have dominated the wetlandvegetation in the immediate vicinity of the site, witha decrease in both as Leptospermum took precedence(Fig. 4). Approximately one-half of New Zealand'snumerous fern species (211) have monolete spores(Large & Braggins 1991), most of which are difficultto differentiate in fossil deposits.

The lack of charcoal fragments in almost all of thepeaty sections of the domain auger deposits indicatesa low frequency of regional fires, suggesting a moistclimate for the Auckland region at the time (Fig. 3,4). The Metrosideros and possible Dacrydium woodin the profiles may be from roots of trees growingon nearby drier crater slopes or on the less wet,subsequent surface of the auger sites (see below).

The change from peat to silty clay deposits inthe more complete profile, HA1, is accompanied bycharcoal and major changes in vegetation, notablya decline in Agathis, Metrosideros, and all wetlandtaxa and an increase in taxa that indicate opening ofthe forest canopy (Fig. 3). The increase comprisesa successional sequence of shrubs and small trees,namely, Elaeocarpus followed by Ericaceae andespecially Myrsine, and finally Hebe. Fuscosporaand Poaceae also increase. The changes could beinterpreted as a decline in conifer-hardwood forest,increased shrub/grassland and Fuscospora forest,and lowering of the water table in the crater wetlandas a result of a change to a cooler and drier climatewith a higher fire frequency (ignited by lightning).The timing of this according to the radiocarbon dates(i.e., after 47 000 yr BP) is consistent with otherpollen records from the Auckland region whichsuggest that beech forest expanded c. 50 000 yr BPand remained dominant until around c. 20 000 yr BP(Lancashire et al. 2002; Sandiford et al. 2002,2003;Shane & Sandiford 2003; Newnham et al. 2007).From c. 23 000 to 16 500 yr BP, continued coolingrestricted Auckland forest to patches within exten-sive shrubland/grassland. However, the amounts ofFuscospora pollen in our profile (<11%) are verylow compared to those of the other Auckland pollenstudies after c. 40 000 yr BP (c. 20-70%). Althoughthis may be partly a percentage effect caused bythe corresponding high Myrsine percentage (up to

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c. 35%) in the profile, the most likely explanationis that the period between at least c. 40 000 and15 000 yr BP is missing, presumably because thereis a hiatus between deposition of the peat and siltyclay. As well as lack of LGM peat formation due toa lower water table, existing surface peat may havebeen lost in the drier conditions (oxidation, wind).A lake environment would likely have preserved theLGM; lack of lake sediments in our profiles suggeststhat a paleo-maar was not formed or preserved,due to the crater having been breached. Thus, thepollen evidence of cooler and drier conditions inour profile may represent the very late glacial en-vironment, when Fuscopsora had declined. This isunlike paleo-maar sites in Auckland, and more likeseveral other North Island sites which preserve littleinformation from cooler, drier periods (Mildenhall1992; Newnham 1999; Horrocks et al. 2007a).

At Auckland Domain, natural infilling of thecrater contributed to the fall in the water table. Theopening of the forest canopy on the crater wallsresulted in an increased erosion rate, with clay/siltprogressively washed into the wetland from the cra-ter slopes and burying the peat deposits. The HA6profile also shows some of these changes, for ex-ample, the Leptospermum and cyperaceae decline,although here the vegetation succession is precededby an increase in Dacrycarpus trees (Fig. 4). Thisis interpreted as Dacrycarpus invading the wetlandto form swamp forest in that part of the wetland asa result of the lower water table (excessively wetsubstrates limit growth).

Post-LGM changes, probably after c. 16 500yr ago as the climate ameliorated, are apparent inthe uppermost few samples of the HA1 profile andinvolve increases in taxa preferring warmer, wet-ter conditions. These are Metrosideros, Ascarina,Cyathea tree ferns, and monolete fern taxa (Fig. 3).Dacrycarpus trees prefer swampy conditions andappear to have invaded the HA1 area with the re-turn to a wetter substrate, as also evidenced by thesmall increase in cyperaceae pollen. The coincidentpresence of taxa indicating early Polynesian andsubsequent European landscape disturbance, notablyKnightia, Freycinetia, Pteridium, Anthocerotae,Taraxacum type, Poaceae, and Pinus, indicate ex-treme compression of the last c. 10 000 yr in thedomain record. This is also evidenced by our dateof 7332 ± 30 yr 14c BP of material from immedi-ately below these changes in HA1, millennia tooold for human impact in New Zealand. The datedmaterial is presumably contaminated with oldercarbon from slopewash. The pollen evidence from

Lake Pupuke (on Auckland's North Shore), whichhas high resolution tephra and radiocarbon control,indicates that large-scale deforestation by fire in theAuckland area occurred c. 700 yr BP (Horrocks etal. 2005a). Human occupation of New Zealand isgenerally thought to have occurred no earlier thanthis approximate date (Higham & Jones 2004). Thecompression is probably due to lack of post-LGMpeat formation and human disturbance, especiallydraining and levelling of the wetland in historictimes.

Age control of the Pukekawa pollen profiles islimited by lack of tephras, a probable hiatus includ-ing the LGM, subsequent lack of peat formation,and extreme compression of the Holocene. Thelack of tephras and non-preservation of the LGM isunusual compared with most other pollen recordsfrom Auckland.

ACKNOWLEDGMENTS

The project was funded by Auckland city council.We thank Ngati Whatua o Orakei and Ngati Paoa forsupporting the project.

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