OFR 151.pdf - CRC LEME

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southeastern Australia than elsewhere in Australia (M.K. Macphail and A.D. Partridge unpubl. data). Exceptions are mainly taxa whose NLRs are confined to cool temperate rainforest, e.g. Dacrydium and Nothofagus, and one now widespread family of herbs (Stylidiaceae), which first occurs in Tasmania during the Eocene-Oligocene transition (Macphail and Hill 1994). Whether the north-west bias implies that northern Australia was a main point of entry, or the region was a centre of speciation during the Late Cretaceous and Tertiary is uncertain. More generally, times of first occurrence are likely to reflect the vagility of the parent plants as well as climatic forcing. 7.3.4 Plant competition and climatic change Factors contributing to the competitive success of the major plant taxa inhabiting the continent included climatic change, the impact of deep leaching on soil fertility, disturbance due to tectonism and volcanism, and (Late Tertiary) herbivory. Because of northward drift of the continent, low light intensities during winter are unlikely to have been a significant limiting factor except possibly in Tasmania during the Danian, whilst the amount and seasonal distribution of rainfall replaced temperature as the major environmental forcing factor during the Late Palaeogene and Neogene except at high elevations. During the Palaeogene, angiosperms largely replaced gymnosperms as the canopy dominants in rainforest over much of the continent. Only the Podocarpaceae with functionally broad leaves were able to compete successfully with angiosperms in the low-light environment within the forest canopy (Brodribb and Hill 1997, Hill and Brodribb 1999). Araucariaceae and Cupressaceae, which lack flattened foliage, remained fairly common only in less shaded habitats. Hill (1990a, 1998a, 1998b) has proposed that sclerophyll species evolved originally in response to low fertility soils in rainforest environments during the Palaeogene, and the morphological expressions of sclerophylly subsequently pre-adapted these plants to reduced or increasingly seasonal rainfall. As aridity became more severe during the Neogene, sclerophyllous plants evolved xeromorphic adaptations to prevent water loss; predominantlymesic biomes such as rainforest gave way to more xeric/open biomes such as sclerophyll forests, woodlands and savannah. The same xeromorphic adaptations may have adapted sclerophyllous plants to withstand the cool-cold (microtherm) conditions that began to develop at high elevations during the Late Oligocene or Early Miocene, and also may have contributed to the probable increased incidence of wildfires at lower elevations during the Late Neogene. 7.3.5 Climatic indicators The Tertiary differs from the Cretaceous in that a significant number of macrofossil and microfossil species can be assigned to extant genera with a moderate to high degree of confidence. As for the Late Cretaceous, key climatic indicator taxa are araucarians, podocarps, palms (Palmae), Nothofagus, Anacolosa and other mesotherm-megatherm taxa although it is recognised that the ecological preferences and tolerances of these and most taxa will have changed (possibly narrowed) to a lesser or greater degree during the Tertiary. For example, Nothofagus (Brassospora)-dominated microfloras are more likely to represent rainforest growing under warm (lower mesotherm) conditions than the cool (microtherm) conditions preferred by most living Nothofagus spp. Typically megathermal taxa such as palms are able to survive under mean annual temperatures as low as 14 ° C (lower mesotherm) as long as the annual temperature range is very low (Wolfe 1987). Accordingly, where other data indicate a more extreme temperature range, fossil palm pollen such as Dicolpopollis, Longapertites and Spinizonocolpites is reliable evidence for very warm to hot (upper mesotherm-megatherm) conditions. 87
Palaeo-distribution data can allow the ecological preferences of a number of commonly occurring to rare taxa to be deduced with some confidence in qualitative terms (Table 7). However, there are compelling reasons why it is premature to use the same data to reconstruct past climates in quantitative terms (cf. Taylor et al. 1990, Sluiter 1991, Greenwood and Wing 1995, Jordan 1997a, Macphail 1997b): (1) The present-day distribution of many plants reflects anthropogenic effects or conditions that are unique to the Late Quaternary. For example, several endemic gymnosperms and ferns in Tasmania have failed to recapture habitats vacated during the Last Glaciation (Macphail 1986, 1997c). (2) Plant successions can be initiated or shaped by non-climatic factors. One example is volcanism whose impacts often mimic those of aridity (Harris and Van Couvering 1995) and the same may be true of frequent wildfires, decreasing soil fertility, forest pathogens and herbivory (references in Van der Putten 2000). (3) Many Tertiary taxa co-occur in associations or communities that have no modern analogue, or which included extinct ecotypes. An example of the latter is the alpine shrub conifer Microcachrys tetragona, now the sole surviving species of a clade that was very widely distributed during the Mesozoic (Dettmann 1994) and Tertiary (Macphail et al. 1993, Jordan 1994, 1997a). Table 7: Inferred climatic preferences of selected Tertiary taxa. FOSSIL TAXON MODERN EQUIVALENT INFERRED CLIMATIC RANGE Mosses, ferns and fern allies Cyatheacidites annulatus Lophosoria upper microtherm to lower mesotherm Matonisporites ornamentalis Dicksonia antarctica upper microtherm to lower mesotherm Polypodiaceoisporites sp. Pteris upper mesotherm to megatherm Stereisporites spp. Sphagnum ±microtherm Trilites tuberculiformis Dicksoniaceae, Matoniaceae microtherm to ?megatherm Gymnosperms Araucariacites australis Araucaria lower? to upper mesotherm Dacrycarpites australiensis Dacrycarpus upper microtherm to lower mesotherm Dilwynites spp. Agathis/Wollemia lower? to upper mesotherm Lygistepollenites balmei Dacrydium (extinct lineage) upper microtherm to lower mesotherm L. florinii Dacrydium upper microtherm to lower mesotherm Microcachrydites antarcticus Microcachrys upper microtherm to lower mesotherm Podocarpidites spp. Podocarpus-Prumnopitys microtherm to ?megatherm Angiosperms Anacolosidites spp. Anacolosa upper mesotherm Australopollis obscurus Callitriche upper microtherm to lower mesotherm Bluffopollis scabratus Strasburgeria upper mesotherm Canthiumidites bellus Randia s.l. ±upper mesotherm Cupanieidites sp. Cupanieae (Sapindaceae) lower to upper mesotherm Gothanipollis spp. Loranthaceae lower to upper mesotherm Granodiporites nebulosus Embothrium upper microtherm to lower mesotherm Ilexpollenites spp. Ilex lower mesotherm to megatherm Haloragacidites harrisii Gymnostoma lower mesotherm to megatherm Intratriporopollenites notabilis Tiliaceae incl. Brownlowia upper mesotherm to megatherm Longapertites spp. Palmae upper mesotherm? to megatherm Malvacearumpollis spp. Malvaceae lower to upper mesotherm Myrtaceidites parvus-mesonesus non-eucalypt Myrtaceae lower to upper mesotherm Nothofagidites asperus, Nothofagus (Lophozonia) upper microtherm to lower mesotherm N. brachyspinulosus Nothofagus (Fuscospora) upper microtherm to lower mesotherm N. emarcidus-heterus, N. falcatus Nothofagus (Brassospora) upper microtherm to lower mesotherm N. endurus, N. senectus Ancestral Nothofagus upper microtherm to lower mesotherm N. flemingii Nothofagus (Nothofagus) upper microtherm to lower mesotherm Nupharipollis spp. Palmae upper mesotherm to megatherm Perisyncolporites pokornyi Malpighiaceae lower to upper mesotherm Polyadopollenites cf. granulosus Archidendron-type lower to upper mesotherm Santalumidites cainozoicus Santalaceae lower to upper mesotherm Sapotaceoidaepollenites spp. Sapotaceae lower to upper mesotherm Spinizonocolpites prominatus Nypa upper mesotherm to megatherm Tricolpites thomasii Loranthaceae lower to upper mesotherm Zonocostites ramus Rhizophoraceae upper mesotherm to megatherm 88
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CRCLEME Cooperative Research Centre
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Electronic copies of the publicatio
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and, for Tertiary continental seque
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2. Analysis of a Plio-Pleistocene l
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Table A (cont.) Basin and related s
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Figure A: Generalised climatic curv
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Carpenter, R.J., Hill, R.S., Greenw
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Hill, S.M., Eggleton, R.A. and Tayl
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Macphail, M.K. and Stone, M.S., 200
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Swenson, U., Backlund, McLoughlin,
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EXECUTIVE SUMMARY This review prese
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Temperature Climates in palaeo-sout
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SUMMARY OF INFERRED CRETACEOUS PALA
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INTRODUCTION Mineral resources, whe
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Professor B. Balme (Geology Departm
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Section 7 (Tertiary climates) This
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vegetation. Moreover, individual ta
Page 37 and 38: 1.3 Flora, vegetation and climate 1
Page 39 and 40: TABLE 2: Classification of vegetati
Page 41 and 42: Figure 2: Relationship of different
Page 43 and 44: Accordingly, only at sites with exc
Page 45 and 46: 2.1.3 Palaeoecology Palaeoecology i
Page 47 and 48: wind-pollinated trees and shrubs bu
Page 49 and 50: 1. The usual practice of equating t
Page 51 and 52: 1. Palaeontological evidence Like p
Page 53 and 54: 5. Facies architecture and lithostr
Page 55 and 56: Subsequent developments include mel
Page 58 and 59: SECTION 4 (GEOGRAPHIC BOUNDARIES AN
Page 60 and 61: SECTION 5 (EARLY CRETACEOUS CLIMATE
Page 62 and 63: events on other continents and sugg
Page 64 and 65: If these considerations apply to th
Page 66 and 67: surrounding basins. Thick sands ero
Page 68 and 69: Haig and Lynch 1993, Erbacher et al
Page 70 and 71: SECTION 6 (LATE CRETACEOUS CLIMATES
Page 72 and 73: has highlighted the roles played by
Page 74 and 75: 6.4.2 Palaeobotany Cenomanian flora
Page 76 and 77: Palaeo-southern Australia Dryland c
Page 78 and 79: 6.7 Time Slice K-6. Late Campanian-
Page 80 and 81: 7.1. Global backdrop SECTION 7 (TER
Page 82 and 83: Explanations for the PETM are centr
Page 84 and 85: East Antarctica and strengthening o
Page 86 and 87: amplifying, pacing and potentially
Page 90 and 91: 7.4 Time Slice T-1. Paleocene [65-5
Page 92 and 93: Palaeo-southern Australia Unlike no
Page 94 and 95: Palaeo-central Australia As for the
Page 96 and 97: 7.6.2 Palaeobotany The palaeobotani
Page 98 and 99: Zone microfloras imply temporary wa
Page 100 and 101: in the Bass Basin, the basal Seaspr
Page 102 and 103: Similarly it is difficult to summar
Page 104 and 105: However, the data are emphatic that
Page 106 and 107: margin of plateau were cooler (~7 0
Page 108 and 109: fossil taxa that are morphologicall
Page 110 and 111: during Late Pleistocene glacial max
Page 112 and 113: SECTION 8 (CONCLUSIONS) Climatic in
Page 114 and 115: • On present indications, Early C
Page 116 and 117: TABLE 8a: INFERRED CRETACEOUS PALAE
Page 118 and 119: 8.2 Results in prospect (recommenda
Page 120 and 121: The 10 μm sieved, oxidised extract
Page 122 and 123: phenology. The method also provides
Page 124 and 125: SECTION 9 (REFERENCES) Acton, G.D.
Page 126 and 127: Ashley, P.M., Duncan, R.A. and Feeb
Page 128 and 129: Birks, H.J.B. and Gordon, A.D., 198
Page 130 and 131: Burnham, R.J., 1989. Relationships
Page 132 and 133: Clarke, J.D.A., 1994. Evolution of
Page 134 and 135: Dettmann, M.E. and Playford, G., 19
Page 136 and 137: Evans, P.R., 1970b. Palynology of H
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Godthelp, H., Archer, M., Cifelli,
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Harris, W.K., 1974. Biostratigraphy
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Hill, R.S., 1994b. Nothofagus smith
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Holland, S.M. and Patzkowsky, M.E.,
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Australia: paleoceanographic implic
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Lindsay, J.M. and Harris, W.K., 196
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Macphail, M.K., Colhoun, E.A. and F
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McGowran, B. and Beecroft, A., 1985
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Morgan, R., 1977. Palynology of Ter
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Abstracts of the Annual General Mee
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Raymo, M.E., Grant, B., Horowitz, M
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Sereno, P.C., 1999. The evolution o
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Taylor, G., 1998. Prediction of mod
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Webb, L.G., 1968. Environmental rel
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Zachos, J.C., Stott, L.D. and Lohma
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APPENDIX 1 CRETACEOUS DATA 167
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1. TIME SLICE K-1 Age Range: Berria
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Australian assemblages, located on
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2. Officer Basin Dinoflagellates in
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2. TIME SLICE K-2 Age Range: Aptian
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Inferred climate The combined data
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Dettmann et al. (1992) have argued
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3. TIME SLICE K-3 Age Range: Cenoma
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3.2.2 North-East Australia 1. Carpe
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4. TIME SLICE K-4 Age Range: Turoni
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1. Otway Basin Limited data (Macpha
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5. TIME SLICE K-5 Age Range: Early
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Inferred climate The data indicate
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6. TIME SLICE K-6 Age Range: Late C
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Contrary to global cooling trends d
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Inferred climate The relatively goo
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Inferred climate As for regions to
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APPENDIX 2 TERTIARY DATA 201
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1. TIME SLICE T-1 Age Range: Paleoc
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also include relatively frequent No
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Inferred climate Some differences b
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Microfloras preserved in the Lower
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subtropical affinities are rare, hi
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2. TIME SLICE T-2 Age Range: Early
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Inferred climate Climates appear to
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northern New South Wales. The assem
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2.2.5 Central southern Australia Ha
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a number of distinctive Proteaceae
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Inferred climate The Regatta Point
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3. TIME SLICE T-3 Age Range: Middle
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2. Lake Torrens Basin Abundant leaf
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Dominance is highly variable. For e
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types (M.K. Macphail unpubl. data).
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Dacrycarpus), Euphorbiaceae (Austro
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(possibly upper mesotherm) and drie
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Basin) on the Eyre Peninsula (Alley
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explanation is that a warm water gy
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several taxa, which first appear in
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4. TIME SLICE T-4 Age Range: Oligoc
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Inferred climate The southern limit
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The lowest and possibly the oldest
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Dominants include fresh to brackish
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Based on the relative abundance of
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(Morgan 1977, McMinn 1981a, Martin
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common (up to 5-6%) in the middle s
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Polypodiaceae, Palmae (Dicolpopolli
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Strasburgeriaceae. Proprietary info
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Rare taxa which first appear in the
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Correlative microfloras in the onsh
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impression of floristic impoverishm
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(Lophosoria) reached Tasmania befor
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2. Otway Basin Oxygen isotope strat
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5. TIME SLICE T-5 Age Range: Late M
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Casuarinaceae, Cunoniaceae, Elaeoca
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maximum temperature of the hottest
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Nothofagus-gymnosperm temperate rai
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5.2.7 Tasmania Late Neogene sedimen
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