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The Miocene Climate in New Zealand: Estimates from Paleobotanical Data

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The Miocene Climate in New Zealand: Estimates from Paleobotanical Data Palaeontologia Electronica palaeo-electronica.org The Miocene climate in New Zealand: Estimates from paleobotanical data Mike Pole ABSTRACT Miocene New Zealand was a small, highly oceanic landmass which makes it ideal for recording terrestrial climate, free of the complications of a continental setting. Fortu- nately, it has a good Miocene fossil record, both marine and terrestrial. This paper reviews past conclusions about Miocene climate then attempts to derive some key cli- mate indices for the period using a variety of plant fossil proxies. The paper looks at three slices of Miocene time – a broad early to earliest middle Miocene time, a restricted period in the middle Miocene, and broader middle–late Miocene. The results suggest early to earliest middle Miocene Mean Annual Temperatures (MATs) reached at least 17–18°C, thus, about 6–7°C warmer than today (coastal areas of southern New Zealand today have a MAT of about 11°C). At times Miocene MAT may have reached 19–20°C. These figures support the cooler estimates of New Zealand Mio- cene climate that have been made previously by using palebotanical proxies, rather than those based on marine invertebrates. Based on plant fossils there is no evidence that New Zealand ever reached truly ‘tropical’ (i.e., megathermal) conditions (> 24– 25°C). The climate in the middle Miocene is confounded by signs of precipitation and temperature change, and the rarity of leaf fossils. However, the data suggest both cool- ing and drying from the early Miocene. The presence of crocodiles yet the disappear- ance of palms, suggests a MAT that was at the lower end of existence for both of these groups, perhaps about 14°C. By the late Miocene, there is evidence for significant cooling, both from leaf size and a drop in plant diversity, which resulted in vegetation dominated in many places by Nothofagus. Mike Pole. Queensland Herbarium, Brisbane Botanic Gardens Mt Coot–tha, Toowong, Qld, Australia, [email protected] Keywords: foliar physiognomy, leaf size; paleobotany; climate change; fire PE Article Number: 17.2.27A Copyright: Palaeontological Association July 2014 Submission: 2 November 2013. Acceptance: 20 June 2014 Pole, Mike. 2014. The Miocene climate in New Zealand: Estimates from paleobotanical data. Palaeontologia Electronica Vol. 17, Issue 2;27A; 79p; palaeo-electronica.org/content/2014/780-miocene-climate-of-new-zealand POLE: MIOCENE-CLIMATE-OF-NEW-ZEALAND INTRODUCTION ther south than Tasmania. Only southern Patago- nia lies at an equivalent latitude. This puts New The Miocene covers a very broad range of Zealand largely under the influence of both the global climate conditions (e.g., Miller et al., 1991; rain–bearing westerly winds and also the drying Zachos et al., 2001). For example, the earliest mid- high pressure cells (Sturman and Tapper, 2005). At dle Miocene includes the ‘Miocene Climatic Opti- times the high pressure cells halt in their usual mum’ – one of the warmest periods in the easterly tracking and remain motionless in the Tas- Cenozoic (Flower and Kennett, 1994; Böhme man – a phenomenon known as “blocking” 2003) that in itself appears to cover a series of dis- (Baines, 1983) and leading to drought. tinct climate fluctuations – ‘The Miocene Oscilla- The Southern Alps are an important control on tion’ (McGowran and Li, 1994). This was followed, the rainfall within New Zealand. They greatly shortly after, by one of the most important climatic enhance rainfall to the west, causing rapid weath- changes of the Cenozoic – a sharp drop in global ering and loss of nutrients from soils, and cause a temperature related to a major increase of ice on rain shadow to the east. New Zealand is also East Antarctica (Shackleton and Kennett, 1975; strongly affected by El Nino Southern–Oscillation Verducci et al., 2007). By the close of the Miocene events. Drought is common east of the Alps, and the West Antarctic Ice Sheet had begun to form as heavy rainfall events are common. Cyclones from global conditions continued to deteriorate (Zachos more tropical latitudes periodically end their move- et al., 2001). Deeper understanding of the mecha- ment over the North Island and cause very intense nisms of these changes is a goal of global climate rainfall events. modeling. Mean annual temperatures (MAT) at sea level New Zealand is a small landmass today with a in New Zealand ranges from about 16°C in the far mostly oceanic climate. In the mid–Cenozoic it was north, to around 9°C on Stewart Island (unless oth- probably even smaller (the shoreline was regress- erwise stated, current temperatures are taken from ing through the Miocene after peak submergence the Worldclim version 1.4, 2.5 minute grid, Hijmans in the late Oligocene–earliest Miocene, Wilson, et al., 2005). Central Otago, at about 45 °S (where 1956; Landis et al., 2008), and with a much more many of the Manuherikia Group fossil assem- reduced topography than it has now. Without the blages described here come from), lies in an inland complicating effects of a large land areas and high and mountainous region, and consequently has a topography, its climate would have reflected the strongly continental character of climate. However, global zonal situation more closely. That gives a the much more equable climate at the coast at the particular relevance to the fossil vegetation of New same latitude has a MAT of about 11°C. Zealand in providing clear reference points for global climate (especially temperature) and atmo- Previous Estimates for Miocene Climate in New spheric circulation patterns (especially rainfall). It is Zealand also located in a key, mid-latitude location, Paleoclimate estimates for New Zealand between the Equator (where the Cenozoic tem- should be put into two important contexts. Firstly, perature changes have been controversial) and the New Zealand lay at somewhat higher latitudes in South Pole, where the Miocene saw significant the early Miocene than today (e.g., Veevers et al., growth of the Antarctic ice sheet (Florindo and Sie- 1991). At 20 Ma Central Otago lay at about 48 °S gert, 2009). (i.e., around 3° higher, using GPlates, www.earth- The aim of this paper is to review the pub- byte.org, with the Müller et al., 2008 rotation lished conclusions for Miocene climate in New model). If New Zealand lay in this position today it Zealand and then to incorporate data from a range might be expected to be a little cooler, although it is of fossil plant taxa in the light of more readily avail- noted that current MATs of the Snares and Bounty able databases and to compare results derived Islands that lie at this latitude are about 10–11°C from independent paleoclimate techniques. Of par- (milder than Stewart Island). A figure of around ticular interest is a re-evaluation of warmth in New 10°C can be regarded as a base against which Zealand during the Miocene Climatic Optimum. most of the estimates for fossil assemblages can New Zealand Climate Today be compared. It would also be more strongly influ- enced by the westerly winds and polar fronts (the New Zealand lies in mid-latitudes, with the effect of the High Pressure cells would be less) and southern part, including the location of the would thus be expected to have more continuous Manuherikia Group (Douglas, 1986), one of the rainfall and fewer drought periods. prime sources of Miocene plant fossils, lying fur- 2 PALAEO-ELECTRONICA.ORG Secondly, during the Miocene New Zealand’s Guinea, whereas those producing ‘fusca’ and topography was considerably lower. The current ‘menziesii’ forms are restricted to cooler Australia, major mountain range in New Zealand, the South- New Zealand, and South America (unfortunately ern Alps, are essentially a Plio-Pleistocene feature there is no place where all three coexist today, like (Sutherland 1995, 1996; Youngson et al., 1998; they apparently did in the past). McQueen et al. Chamberlain et al., 1999). It follows that significant (1968) argued that the three Nothofagus groups rain shadows would have been absent, and the are favoured by different climates. The N. “brassii’ other extreme of very high rainfall (with attendant group, were taken to indicate a climate of “constant rapid leaching of soil nutrients) would have been humidity and one warmer than that occupied by the absent, too. However, buried early Miocene topog- N. “fusca’ group,” with the N. ‘menziesii’ group indi- raphy within the Manuherikia Group of more than cating the coolest conditions. This meant that the 400 m is known (Douglas, 1986) and perhaps total relative proportions of the pollen of these three topography – i.e., what lay around the edge of the groups could then be used to estimate climate. The basin, is likely to have been higher. This topogra- presence and abundance of other pollen types pro- phy is likely to have had some ecological signifi- vided additional evidence for the climate. For cance. Assuming a lapse rate of around 0.65°C per instance Bombacacidites bombaxoides (Bombax) 100 m (Meyer, 1992; Wolfe, 1992), there would and Cupanieidites (representing a clade within have been significantly reduced temperatures on Sapindaceae) were taken as indicators of relative the uplands than on the valley floors, and poten- warmth. The abundance of Podocarpaceae pollen tially distinct vegetation. Added to this may have was noted whilst common proteaceous pollen was been the ‘Massenerhebung’ phenomenon (Grubb, also used to suggest seasonal rainfall. Based on 1971; Flenley, 1995). This is found in the geo- these arguments, McQueen et al. (1968) noted that graphic tropics today, but if it operated in the early pollen of the Nothofagus “brassii’ group was domi- Miocene at higher latitudes, it may have produced nant over the N. “fusca’ group from the latest Oligo- a distinct cloud forest vegetation on low peaks.
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