Spinescence is an important functional trait possessed by many plant species for physical defence against mammalian herbivores. The development of spinescence must have been closely associated with both biotic and abiotic factors in the geological past, but knowledge of spinescence evolution suffers from a dearth of fossil records, with most studies focusing on spatial patterns and spinescence-herbivore interactions in modern ecosystems. Numerous well-preserved Eocene (~39 Ma) plant fossils exhibiting seven different spine morphologies discovered recently in the central Tibetan Plateau, combined with molecular phylogenetic character reconstruction, point not only to the presence of a diversity of spiny plants in Eocene central Tibet but a rapid diversification of spiny plants in Eurasia around that time. These spiny plants occupied an open woodland landscape, indicated by numerous megafossils and grass phytoliths found in the same deposits, as well as numerical climate and vegetation modelling. Our study shows that regional aridification and expansion of herbivorous mammals may have driven the diversification of functional spinescence in central Tibetan woodlands, ~24 million years earlier than similar transformations in Africa.
Plant functional traits refer to plant characters that impact plant survival, growth, or reproduction1,2, which in turn have significant influences on ecosystem processes3,4. Functional traits enable plants to better acquire and retain resources, promote niche differentiation, and reduce interspecific competition, while functional trait redundancy maintains the stability of ecosystem function5,6,7. Although most studies focus on the role of functional traits in structuring modern ecosystems8,9,10, little is known about how these functional traits evolved in the geological past, particularly under varied environmental stressors. Plant functional traits are shaped by the interaction between plants and the surrounding environment, including faunal interactions, during the long process of evolution in deep time1; therefore, it is crucial to investigate the evolutionary history of plant functional traits to better understand the mechanisms moulding them.
Spinescence (a general term for the phenomena of spines, prickles, and thorns on plants) is an important functional trait shared by numerous plant families worldwide and mainly provides physical protection against vertebrate herbivores11,12. Sharp spines can hurt the bodies and mouthparts of herbivores, and thus restrict their feeding rates13. In general, spine architecture and spatial distribution are largely influenced by mammal herbivory and correlate strongly with the spatial distribution of megaherbivores13,14,15,16. Both prickles and thorns can defend against herbivores and even climbing mammals17, but whether they have other functional properties is unclear. Today, spinescence is common in open habitats with abundant herbivores and relatively arid climates, such as savanna, featuring an open tree canopy with a grassy understory18,19,20.
To better understand mechanisms underlying the evolution of plant spines, it is necessary to explore their occurrence in deep time. Spiny plants in Africa, evidenced by both plant and mammal phylogenies, underwent a massive radiation during the early Miocene, particularly in African savannas18, which are characterised as open-canopied ecosystems. Spiny species have been linked to the arrival and diversification of bovids from Eurasia during the Neogene, as well as climatic drying in Africa that promoted the development of open vegetation18,21. Even though spiny plants are distributed worldwide, our understanding of their evolutionary history remains woefully incomplete.
Fossils of plant spines are physical evidence for the presence of plant spinescence at the place and time the plant was alive; nevertheless, they have been largely ignored and scarcely reported compared to other plant organs, such as leaves, fruits, and seeds. Previously, spiny fossils have been largely overlooked in fossil floras, with a few exceptions such as the Eocene Green River flora22 and Oligocene Bridge Creek flora23,24 of North America, and the Miocene Tortonian flora25 of Europe. Overall, their occurrence in fossil floras is not well documented and the ecological and evolutionary significance of these scattered spiny fossils have never been explored at continental scale.
Here we report exceptionally rich assemblages of spiny plant fossils collected from late Eocene (~39 Ma) sediments in central Tibet (Fig. 1). The Tibetan region has undergone dramatic evolutionary and climatic change since the collision of the Indian and Eurasian plates began between 65–55 Ma26,27,28,29,30. Habitat differentiation favoured the diversification and turnover of plant and mammal species31,32 as central Tibet changed from hosting a closed subtropical humid lowland forest valley ecosystem during the middle Eocene33 to the open and dry highland steppe of today34. These spiny fossils together with phytoliths and plant megafossils, including those of monocotyledonous herbs and dicotyledonous woody species, point to an initial opening-up of the vegetation as early as the late Eocene in central Tibet. Combined with molecular phylogenetic analyses, we document the early diversification history of spiny species in Eurasia. Using proxy and modelling data, we reconstruct the vegetation, climate and herbivory that favoured spiny plant evolution in the Eocene of central Tibet.
We document a total of 44 spine-bearing fossil specimens collected from two fossil localities (Fig. 1, Supplementary Fig. 1): the Dayu locality (32° 20′ N, 89° 46′ E), within the middle member of the Niubao Formation, is considered to be ~39 Ma (Bartonian, early late Eocene) based on radiometric (U/Pb) dating35,36, while the other site at Xiede (31° 58′ N, 88° 25′ E) we consider age-equivalent as it contains a wide range of similar fossils in addition to spine-bearing plants. Both localities are within the central Tibetan Bangong-Nujiang Suture Zone.
Spine morphology is here divided into prickles (modified epidermis) and thorns (modified axial stems). According to size and growth pattern, we classify prickles into two types and thorns into five types. Further details are given in Supplementary Figs. 2–8, Supplementary Note 1.
Morphotype I (Fig. 2b) Prickles arranged on stems alternately. The average length of prickles is 4.9 ± 1.6 mm. The mean width at the base of each prickle is 5.8 ± 1.2 mm. Each prickle curves upward at an angle between 45° and 90°.
Morphotype II (Fig. 2e) Prickles occur on stems irregularly. The average length of prickles is 3.8 ± 1.2 mm. The mean width at base of each prickle is 5.2 ± 1.5 mm. The prickles grow almost perpendicular to the stem.
Morphotype III (Fig. 2h) Thorns grow on stems oppositely and densely. The average length of thorns is 5.6 ± 2.1 mm. They grow on the stem at an angle of ~90°.
Morphotype IV (Fig. 2i) Thorns grow on stems alternately. The average length of thorns is 4.7 ± 1.7 mm. Each thorn curves slightly upwards or downwards.
Morphotype V (Fig. 2d) Thorns grow on stems alternately. The average length of thorns is 29.0 ± 14.7 mm. They grow on the stem at an angle of ~90°.
Morphotype VI (Fig. 2j) Thorns grow on stems alternately and at an acute angle of less than 45°. The average length of thorns is 5.9 ± 1.4 mm.
Morphotype VII (Fig. 2k) Thorns grow on stems in pairs oppositely. The average length of thorns is 2.6 ± 0.6 mm. They grow on the stem at an angle of ~90°.
Phylogeny of spiny plants
The accumulation curve of spiny eudicots (Fig. 3a) suggests that the first spiny plant species emerged during the Paleogene in Eurasia. This strengthens our findings pointing to an early occurrence of spiny plants in Asia, although fossil spines are generally under-explored over this period. The proportion of spiny plants remained low until 40 Ma, but has risen exponentially since then (Fig. 3a). For approximately 20 Myr after their emergence we estimate that spines occurred in only 2 lineages, but during the late Eocene there was a four-fold increase from 2 to 8 spiny lineages within the next 10 Myr, closely matching the 7 morphotypes found in our fossil records. The beginning of this substantial radiation of spiny plants, estimated according to molecular clock techniques, closely matches the timing of our fossil spines, reinforcing the hypothesised early emergence of spiny plant diversity in Asia. The mid-late Eocene, therefore, witnessed a step change in the abiotic and/or biotic environment of the woody flowering plants in Eurasia.
Palaeoclimate and palaeoelevation
We applied the Climate-Leaf Analysis Multivariate Program (CLAMP) to the Dayu leaf flora (Supplementary Figures 9, 10), which indicates a climate with summers that were warm (warm month mean temperatures of 24–30 °C) and dry (summer vapour pressure deficit (VPD.sum) of 10.2–17.2 hPa), and winters that were cool (cold month mean 0.2–7.2 °C) and moist (VPD.win 2.8–5.8 hPa). Occasional frosts may have occurred but were not harsh, nor prolonged, and thus survivable by palms that also occur in the Dayu section. The dry bulb mean annual temperature of 15.6 °C exceeds, but is close to, the lower survivable limit for palms (14.2 °C)37. The wet/dry precipitation ratio is 4.6:1, suggesting a borderline monsoonal climate. More details are given in Supplementary Tables 1–3.
Both the moist enthalpy and the wet bulb terrestrial lapse rate approaches for palaeoaltimetry38 gave similar results for the elevation of the Dayu fossil assemblage: 2.6 ± 1.2 km and 2.7 ± 0.9 km respectively (Supplementary Note 2).
Numerical climate modelling for central Tibet, with a valley floor set at 2.5 km bounded by 5 km high East-West trending mountain ranges, also indicates a winter-wet warm climate within the valley (a mean annual air surface temperature 23–26 °C, and a cold month mean surface air temperature of 9–11 °C depending on location) with progressively more arid conditions towards the east where some minor summer rain also is predicted (Supplementary Note 3). Note that these model temperatures are slightly warmer than those reconstructed from CLAMP, but the nominal model valley floor elevation is lower than that reconstructed from proxies, and CLAMP is known to return dry bulb temperatures that reflect evapotranspirational cooling in dry regimes where groundwater is plentiful39. Overall, the modelling and proxy thermal regimes are similar, pointing out to drying and cooling climate in central Tibet by the mid-late Eocene accompanied by some within-valley increase in elevation (~1 km) since ~47 Ma33.
Herbaceous plant diversity
Herbaceous fossil specimens of the Dayu flora (n = 315), classified as monocots based on their parallel veins and gross morphology, account for ~38% of all plant fossil specimens found at Dayu. Using leaf size, length, and stem growth form, we were able to classify herbaceous fossils into six morphotypes (Supplementary Fig. 11). Currently, we cannot determine if they were terrestrial or aquatic plants due to limited preservation. However, there are abundant herbaceous phytoliths in the bounding sediments, representing several mainly non-aquatic grass subfamilies, including Chloridoideae and Pooideae (Supplementary Figure 12). The diverse morphology of phytoliths observed from the fossil-bearing outcrops (Supplementary Figure 12) indicates a species-rich grass community within an ecosystem that also contained palms and numerous other woody taxa, but evidence for such a diverse grass component does not occur in older Tibetan floras, e.g., the middle Eocene Jianglang flora from central Tibet33 (Supplementary Fig. 13).
Progression from the older flora to the younger in the Bangor and Lunpola basins shows an increase in phytolith abundance and diversity. The phytolith assemblage from the ~47 Ma Jianglang section, where the megafossils are interpreted to represent a subtropical forest, is dominated by those forms produced by woody taxa, and these greatly exceed grass forms (Supplementary Fig. 13, Supplementary Table 4). Within the lower part of the Dayu section (~39 Ma), phytoliths are still dominated by those produced by woody plants but bulliform phytoliths typically produced by grasses become more common (Supplementary Figure 13). The main fossil-bearing layer higher in the Dayu section preserves not only the numerous spiny taxa but also abundant phytoliths where, among those that could be identified, 66% were produced by grasses and only 34% by woody plants. As grass tends not to grow in abundance in shaded conditions, all these megafossils and phytoliths strongly suggest the progressive development of a semi-open habitat dominated by herbaceous plants with trees forming a broken canopy, such as is seen in modern woodlands40,41. This interpretation is further supported by experiments using fully coupled ocean-atmosphere-vegetation climate modelling with Eocene boundary conditions and a Tibetan Central Valley topography (Supplementary Note 3, Supplementary Fig. 14). These simulations show early Eocene closed forest vegetation transitioning to a more open system by the middle Eocene.
Herbivorous mammal fossils of the Tibetan Plateau
Available fossil records indicate that the regional diversity of large herbivorous mammals increased substantially from the Paleogene to the Neogene (Fig. 3a). Large herbivores were abundant in central Asia after the early Eocene. There are numerous fossil records of Paleogene herbivorous mammals from the Tibetan Plateau and its surrounding regions, mainly represented by Brontotheriidae, Hyracodontidae, Amynodontidae, Paraceratheriidae, and Anthracotheriidae (Supplementary Data 1), and recently a rhino (Plesiaceratherium sp., Rhinocerotidae) was found from the early Miocene strata of the central Tibetan Plateau42. At the broader scale of central Asian countries, we observed a first peak of herbivore diversification in the first half of the Eocene (~50 Ma, Fig. 3a), followed by a second peak between the late Eocene to early Oligocene (~40–28 Ma; Fig. 3a). Most of the second peak species belonged to Perissodactyls (~84%, n = 187), mainly from the Hyracodontidae, Brontotheriidae and Lophialetidae families. While most of the species identified to family level in the late Eocene still belonged to Brontotheriidae, a few species of Hyracodontidae and Lophialetidae emerged, suggesting that these clades may have helped drive the spiny plant diversification reflected by our findings. Among the main changes in the late Eocene-early Oligocene fauna, the proportion of Artiodactyls increased to ~43% (n = 124), Rhinocerotidae, Paraceratheriidae and Lophiomerycidae started to diversify, and finally cervids and bovids appeared (Supplementary Data 1). In addition, many hippo-like amphibious species belonging to Anthracotheriidae, Amynodontidae and Anthracobunidae were present both in the first half of the Eocene and in the late Eocene–early Oligocene, with 30 and 36 species respectively. This is consistent with sedimentological evidence for the presence of water bodies, at least seasonally, which over time became increasingly brackish to saline43. Furthermore, these clades included several very large herbivores that required large amounts of food, both grass and tree leaves. These megaherbivores have been found since in open habitats such as savanna44, adding to our interpretation that increasing herbaceous (predominantly grass) and spiny plants co-existed in an open canopy semi-wooded environment.
The late Eocene diversification of spiny plants and semi-open woodlands in central Tibet
The rich assemblage of spiny plant fossils from the late Eocene (~39 Ma) along the Bangong-Nujiang Suture Zone in central Tibet traces the evolutionary history of spiny plants in Eurasia back to the Paleogene. These fossils evidence an early diversification of spiny plants in the Tibetan region contemporaneous with the emergence of open semi-wooded habitats by the late Eocene, and early in the transition of central Tibet to full plateau formation which appears to have been almost complete early in the Oligocene36.
Based on current knowledge, this late Eocene flora in central Tibet bears the richest diversity of spiny plants known among Cenozoic floras worldwide. The evolutionary history of spiny plants is still poorly known largely due to a dearth of fossil records, which may be because spinescence tends to be most prevalent in semi-arid to arid environments where fossilisation potential is normally low18,45. The rich spine assemblages from Tibet enable us to investigate the morphological diversity of spiny plants in a highly unusual context. The fossils studied here represent both prickles and thorns divisible into seven morphotypes (Fig. 2). Although with only morphological characters it is difficult to assign unambiguously these fossils to specific taxa, these spiny fossils show a range of distinct morphological characters, indicating that a wide variety of spiny species existed in the same community in central Tibet during the late Eocene.
All plant fossil evidence, together with numerical modelling (Supplementary Note 3; Supplementary Fig. 14), indicate that central Tibet hosted a landscape that supported an open habitat, seemingly in the form of woodlands, during the late Eocene. Woodlands are usually considered to be tree-rich communities with open canopies and grassy understories40,41. Today, spiny plants appear to be most abundant in open canopy communities, where predation pressure from mammalian herbivores is high11,18. Numerous fossilised monocots (Fig. 4, Supplementary Fig. 11) and abundant phytoliths (Fig. 4, Supplementary Fig. 12) representing the grass family (Poaceae) and attributable to the subfamilies Chloridoideae, Pooideae, and potentially Bambusoideae point to an open ecosystem46. These well-preserved fossils of herbaceous plants show that the vegetation could not have been dense forest, even though the assemblage inevitably will have been biased towards representing a more tree-rich community bordering the ancient lake shoreline where water was most abundant. This is emphasised by the presence in the region of several amphibious mammals that had a similar niche to modern hippos47 in African savanna. Away from lake margins, the relatively seasonally dry environment would support fewer trees and shrubs and thus more open vegetation. Woody species that have been found preserved in the Dayu section include Koelreuteria lunpolaensis48, Ailanthus maximus49, Cedrelospermum tibeticum50, and several species in Malvaceae and Fabaceae (Supplementary Figs. 9, 10), which are families commonly found in open ecosystems, as well as a palm, Sabalites tibetensis51. Our census of the leaf flora from the same layer at the Dayu site shows that the modern affinities of 10 fossil taxa in the flora belong to families/orders that contain spine-bearing species, i.e., Malvaceae, Rosales, Fabaceae, Ulmaceae, Cannabaceae, Menispermaceae, Simaroubaceae, Anacardiaceae, Myrtaceae, and Araliaceae (Supplementary Table 5). Notably, the plant diversity was much lower than in the earlier middle Eocene (~47 Ma) Jianglang subtropical flora reported recently from the adjacent Bangor (Baingoin) Basin33.
Factors promoting the diversification of spiny plants in central Tibet
The Tibetan Plateau experienced a complex geological evolution, leading to dramatic palaeoenvironmental changes both locally and regionally52,53,54. Although the details of Tibetan orogeny are still being resolved, the latest geological and palaeontological studies have revealed that the plateau did not rise as a single coherent entity55,56,57. A deep East-West trending valley existed in what is now the central Tibetan Plateau for more much of the Paleogene (Fig. 3b), with the valley bottom being at an elevation of ~1500 m at 47 Ma33 and ~2600–2700 m at ~39 Ma (Supplementary Note 2), bounded by the Gangdese and the Tanggula (Qiangtang) highlands with crest heights > 4 km to the south and north58 respectively. It was not until just prior to the Neogene that the modern low relief high elevation plateau formed36,51,59. During the middle Eocene, a warm and humid airflow evidently penetrated the valley, supporting a humid climate and subtropical biota33,54,60. The palaeoclimate of the Dayu flora derived from the CLAMP analysis is similar, but slightly drier, than that experienced by the older Jianglang flora nearby (Supplementary Table 1), and is consistent with an early onset of regional drying that became more pronounced after the end of the Oligocene43. The reduction in growing season precipitation is largely a function of the shorter growing season, but the mean monthly growing season precipitation does indicate slightly drier conditions for the Dayu assemblage.
Undoubtedly, palaeoenvironmental changes during the development of the Tibetan Plateau stimulated an overturn of plant taxa and an opening-up of the vegetation as the floor of the central valley rose in the latter part of the Paleogene and regional drying took place. These changes may have stimulated herbivore access, increased herbivory pressure on plants, and drove the evolution of defensive spines. Moreover, at this time global climate began its transition from a ‘warm house’ to a ‘cool house’ and eventually an icehouse condition61. Nevertheless, the presence of palm fossils in the Dayu flora indicated that the coldest month mean temperature and mean annual temperature in central Tibet at ~39 Ma were not below 5.2 °C and 14.2 °C, respectively51. Temperature, precipitation and solar radiation are major abiotic factors that determine vegetation growth, distribution ranges and dynamic change62. When thermal conditions are sufficient for vegetation growth, water becomes the main limiting factor controlling vegetation status63. During the early late Eocene, central Tibet was an intermontane lowland bounded by mountains that seem to have exceeded 4,000 metres59. Despite the initial influx of moisture, the retreat of the Neotethys during that period resulted in a reduction in the amount of water vapour entering the then shallowing valley, which, together with a growing Himalaya, led to the increasingly dry Neogene environmental conditions across the Tibet and central Asia64. A recent study demonstrates both drying and cooling occurred in central Tibet as the surface elevation of the Tibetan Central Valley increased from ~2.5 km to more than 4 km between 39 Ma and 29 Ma36.
Since open habitats are generally able to carry larger groups of herbivores and these animals have a greater impact on plants whose growth is also limited by reduced rainfall and temperature, herbivore pressure during this period inevitably increased, driving the evolution of defensive spines. Numerous fossils of large herbivorous mammals have been found on the Tibetan Plateau and adjacent regions, evidencing their presence in the Paleogene (Supplementary Data 1). Examples include the late Eocene Brontotheriidae65, Hyracodontidae, late Oligocene Paraceratheriidae66, as well as the early Miocene Rhinocerotidae42. Although many species are now extinct, fossil records show that herbivorous mammals became increasingly diversified, including an important turnover of herbivore families, notably the emergence of bovids and cervids, from the Paleogene to the Neogene (Fig. 3a, the blue curve).
In terrestrial ecosystems, mammalian herbivores influence the length, density, and distribution of plant spines14,67,68. For example, the rapid accumulation of spiny plants in Africa since the middle Miocene closely matched the arrival of bovids18. The earlier emergence of ruminants, and other extant families of herbivores in Eurasia may have triggered the early radiation of spiny plants in Tibet by filtering out the undefended plant species. Mammalian herbivory is a major driver of global vegetation dynamics69, and large animals are thought to have the capacity to create open ecosystems by reducing woody biomass70,71,72. Exclosure experiments conducted in Africa reveal that species-rich megaherbivore communities can effectively reduce woody vegetation coverage by 15–95%73.
The plant fossils reported here record the beginnings of vegetation opening-up under a drying/cooling climate as the modern Tibetan Plateau began to form from the late Eocene onwards, and the observed spinescence marks the early development of defence mechanisms against large herbivore feeding pressure in the region. We infer that in the late Eocene climate changes in central Tibet, driven by the onset of global cooling61 and regional tectonism74, resulted in changes in vegetation that allowed increased access by large herbivores. This in turn led to further opening-up of the landscape favouring further diversification of herbivorous mammals and spiny plants. This string of climate/plant/animal interactions long pre-dated the middle Miocene arrival of herbivorous mammals (especially bovids) in Africa where similarly linked evolutionary feedback processes took place some 24 million years later18.
This research complies with all relevant ethical regulations. The fossil excavation was permitted by Department of Natural Resources and Department of Science & Technology in Tibetan Autonomous Region, China.
Fossils in this study are from the Dayu and Xiede sections, which are located within the Bangong-Nujiang Suture Zone that is aligned roughly East-West through what is now the central Tibetan Plateau. The present average surface elevation of these two fossil sites is about 4700 metres42, and predominantly vegetated by alpine steppe34 (Supplementary Figure 1).
The Bangong-Nujiang Suture Zone hosts thick Cenozoic deposits, the lower part of which in the adjacent Lunpola and Bangor basins comprise the Paleocene-Eocene Niubao Formation and the upper part the Oligocene-Miocene Dingqinghu (Dingqing) Formation75,76,77. The Niubao Formation, up to 3,000 metres thick36, is mainly formed of fluviatile red clastic rocks interspersed with greyish green mudstones and sandstones. Plant fossils have recently been reported from mudstones in the middle part of the formation near the top of the lower member of the Niubao Formation, and include, amongst others, Ailanthus maximus49, Lagokarpos tibetensis78, Illigera eocenica79, and Asclepiadospermum marginatum and A. ellipticum80.
The Dingqinghu Formation is characterised by grey lacustrine mudstones together with sandstones and oil shales, with a total thickness of about ~1,000 metres36,42,76. It bears rich records of animals and plants, including two Oligocene ostracode assemblages: Austrocypis-Cyprinotus-Pelocypris and Ilyocypris-Limnocythere81,82, fishes including Plesioschizothorax83, and mammals such as Plesiaceratherium42.
Fossils in this study are from two sites in the Niubao Formation (Fig. 1). According to recent radiometric dating throughout the Dayu section, the age of the plant fossil horizons in the Dayu section (32° 20′ N, 89° 46′ E) is ~39 Ma36 (Bartonian, early late Eocene). For the other site in Xiede (31° 58′ N, 88° 25′ E), the biota is similar to that at Dayu, and many species are common to both sites, such as a climbing perch Eoanabas thibetana84, a water strider Aquarius lunpolaensis85, and plants, e.g., Limnobiophyllum pedunculatum86, Sabalites tibetensis51, Cedrelospermum tibeticum50, and Ailanthus maximus49. Therefore, we consider both sites to be age-equivalent, dating from the early late Eocene.
In total, 44 spiny fossils were collected from the Dayu and Xiede localities. Among them, 19 specimens are from the Dayu section, and 25 specimens are from the Xiede section, respectively. All specimens are deposited at the Palaeoecology Collections of Xishuangbanna Tropical Botanical Garden (XTBG), Chinese Academy of Sciences. They were photographed with a Nikon D700 digital camera (Nikon, Kanagawa, Japan). A stereoscope (Zeiss Smart Zoom 5) was used to photograph the detailed morphology of the spines at the Central Laboratory in XTBG. Digital photographs of extant and fossil specimens were measured using ImageJ 1.52a software (http://rsb.info.nih.gov.ig/).
The morphological definitions of spines followed Cornelissen2, and Bell and Bryan87. We compared spine morphologies in living eudicots and monocots (Supplementary Fig. 15) to those of our fossils and found that only eudicots exhibit the same spine morphology87 as those of our fossils. We classified fossil spines into prickles and thorns according to two criteria: prickles originate from the epidermis of plant organs such as stems, leaves and petioles, whereas thorns are modified branches and include internal vascular bundles. For fossil specimens, due to the different structures of prickles and thorns, we observed distinct scars at the junction between prickles and stems, but these are absent in thorny species. Secondly, thorns always grow from stem nodes and therefore display a regular phyllotaxy, but prickles tend to be distributed randomly along the internodes.
For morphological comparison of spinescence among modern species, we consulted online data sources including JSTOR Global Plants (http://plants.jstor.org/) and the Chinese Virtual Herbarium (http://www.cvh.org.cn/). Living species of Rubus alceifolius and Xylosma racemosum were collected from XTBG and from the wild in the Xishuangbanna region, Yunnan.
To investigate the emergence and early diversification of spiny eudicots, we reconstructed the evolutionary history of spines across species of woody eudicots represented on the mega-phylogeny of plants from Zanne et al.88 using the make.simmap function in phytools89 and the ape90 and Geiger91 R-libraries (Supplementary Code 1). We coded, as a binary trait, for the presence of spines in plants found in Eurasia (n = 1590 species) mostly using scans from https://plants.jstor.org/. We excluded species when the origin appeared ambiguous between more than one continent. To control for the relatively recent origin and diversification of spines, we allowed rates to vary through time (parameter Δ = 9), and constrained evolutionary transitions to preclude reversals from the spiny to non-spiny state, reflecting the rarity of this evolutionary event, and avoiding potential bias due to the over-representation of non-spiny lineages among woody taxa92.
Palaeoenvironmental reconstruction using Climate-Leaf Analysis Multivariate Program (CLAMP)
We applied CLAMP (http://clamp.ibcas.ac.cn) to the woody dicot leaf forms (24 distinct morphotypes in the Dayu flora, Supplementary Figures 9, 10) with the PhysgAsia2 (http://clamp.ibcas.ac.cn/CLAMP_PhysgAsia2.html) training set and Worldclim2 climate data (http://worldclim.com/version2) calibration74 to derive palaeoclimate metrics. Scoring of the fossil leaves followed the CLAMP protocols. The CLAMP scoresheets are given as Supplementary Tables 2, 3.
Among the palaeoclimate metrics that CLAMP returns in this calibration are moist enthalpy and wet bulb mean annual temperature and both can be used to assess palaeoelevation. The former uses conservation of energy principles, and the latter exploits the reduction in temperature that occurs as a land surface increases in height (a terrestrial thermal lapse rate). Both approaches were used to determine the height at which the Dayu flora existed.
As a parcel of air rises against a mountain front, temperature declines, humidity rises and potential energy increases, but overall the energy it contains is conserved93. This energy is called moist static energy (h) and excludes kinetic energy, which tends to be small except during a hurricane.
where H is moist enthalpy, Z is height, and g is gravitational acceleration (a constant 9.81 cm/s2).
This conservation of energy means that we can exploit the difference in moist enthalpy between two locations (Hlow and Hhigh) to determine the height difference between them, ΔZ, as follows:
Thermal lapse rates describe changes in temperature with changing elevation, and in general (with exception of a temperature inversion) temperature measured at Earth’s surface declines with increasing height and can be expressed as:
where Γε is the terrestrial lapse rate, dT is the change in temperature, and dz is the change in height. We used wet bulb lapse rates because these are more reliable than those based on dry bulb temperatures and are independent of season38. The local terrestrial wet bulb lapse rate was determined from modelling as in Farnsworth et al.38 using a best estimate realistic topography.
Sea level moist enthalpy was derived from model data adjusted to be compatible with CLAMP values using Eocene archived proxy data ranging from northern India to Svalbard, adjusted for palaeolatitude, following the methodology of Su et al.33. Wet bulb temperature at mean sea level was also obtained from the adjusted model data. Further details are given in Supplementary Note 2.
Palaeovegetation predicted by climate modelling
To produce a more applicable, time dependant, simulation of the Dayu environment, we employed a fully coupled Atmosphere-Ocean General Circulation Model (AOGCM), HadCM3BL-M2.1aD94. Model boundary conditions (topography, bathymetry, and ice sheet configurations; at 0.5×0.5° resolution and downscaled to model resolution) for the Bartonian (~39 Ma) are provided by Getech Plc. Stage-specific solar luminosity was calculated using the methods of Gough95. Atmospheric CO2 concentrations were prescribed at 1,120 ppm, consistent with the Phanerozoic CO2 compilation of Foster et al.96. Each experiment was run for 12,422 model years to allow the surface and deep ocean to reach equilibrium and achieve a state with no net energy imbalance at the top of the atmosphere. This is fundamental as ocean circulation can take many thousands of model years to establish its equilibrium state. Climate means were calculated from the last 100-years of each simulation. Time-varying latitude and longitude plate palaeo-rotations were provided for the Dayu location to allow for accurate comparison within the model. Dayu was located at a palaeolatitude of 32° 30′ N, 82° 54′ E using the Getech Plc. plate model. Tibetan orography was constrained to represent high (5 km) Gangdese and Tanggula mountain systems bounding an East-West trending valley system the floor of which was set at 2.5 km (Supplementary Fig. 14A). The dynamic vegetation scheme TRIFFID97,98 (Top-down Representation of Interactive Foliage and Flora Including Dynamics), which predicts the distribution and properties of global vegetation based on plant functional types using a competitive, hierarchical formulation derived from the land-atmosphere climate interactions in the model (TRIFFID was executed and updated every 10 model days) to predict vegetation types likely to existed within the valley (Supplementary Fig. 14B).
Herbaceous plant and vegetation types in the late Eocene
To understand the vegetation type, we assessed the diversity of grass species in the flora. We studied megafossils, pollen grains/spores, and phytoliths indicative of grass from the spiny plant fossil-bearing layer of the Dayu section. Pollen grains and spores were poorly preserved in Dayu and Xiede sections, preventing us from further palynological investigation, but phytoliths were relatively well preserved. The extraction and identification of phytoliths from sediments followed the methods of Strömberg99 and Lu100. The procedure consisted of treatment with 30% hydrogen peroxide (H2O2) and cold 15% hydrochloric acid (HCl), followed by heavy liquid separation using zinc bromide (ZnBr2, density 2.35 g/cm3) and mounting on a microscope slide with Canada balsam. From each extracted sample, at least one slide was prepared for phytolith counts and analysis under a LEICA DM 1000 microscope at 400× magnification. For these samples with poorly preserved phytoliths somewhat less than 100 diagnostic forms were counted (Supplementary Table 4).
Paleogene herbivorous mammal fossils
We used fossil records of all Artiodactyls and Perissodactyls from fossilworks (http://fossilworks.org/) (Supplementary Data 1). Both are orders including mammals that have similar ecological roles as modern ungulates. From fossil records, we built a dataset with the first occurrence of each species using the maximum date estimate as the species are very likely older than the first fossil. This allowed us to deduce a cumulative curve of species (n = 658 species) as an estimate of speciation rate. We focused on the fossil records from countries including and surrounding the Tibetan Plateau, including China, India, Afghanistan, Kazakhstan, Kyrgyzstan, Mongolia, Myanmar, Nepal, Pakistan, Turkmenistan, and Uzbekistan.
Further information on research design is available in the Nature Research Reporting Summary linked to this article.
All data analysed in this paper are available as part of the Article and Supplementary Information. All fossils are deposited at the Paleoecology Collections of Xishuangbanna Tropical Botanical Garden (XTBG), Chinese Academy of Sciences. Additional data related to this paper may be requested from the authors. Correspondence and requests for materials should be addressed to T.S. (email@example.com). Source data are provided with this paper.
Code for phylogeny reconstruction is provided in the Supplementary Information.
Reich, P. B. et al. The evolution of plant functional variation: traits, spectra, and strategies. Int. J. Plant Sci. 164, S143–S164 (2003).
Cornelissen, J. H. C. et al. A handbook of protocols for standardised and easy measurement of plant functional traits worldwide. Aust. J. Bot. 51, 335–380 (2003).
Liu, X. J. & Ma, K. P. Plant functional traits concepts, applications and future directions. Sci. Sin. Vitae 45, 325–339 (2015).
Diaz, S., Cabido, M. & Casanoves, F. Plant functional traits and environmental filters at a regional scale. J. Veg. Sci. 9, 113–122 (1998).
Kraft, N. J. B., Godoy, O. & Levine, J. M. Plant functional traits and the multidimensional nature of species coexistence. Proc. Natl Acad. Sci. USA 112, 797–802 (2015).
Barton, K. E. Tougher and thornier: general patterns in the induction of physical defence traits. Func. Ecol. 30, 181–187 (2016).
Adler, P. B., Fajardo, A., Kleinhesselink, A. R. & Kraft, N. J. B. Trait-based tests of coexistence mechanisms. Ecol. Lett. 16, 1294–1306 (2013).
Wright, S. J. et al. Functional traits and the growth–mortality trade-off in tropical trees. Ecology 91, 3664–3674 (2010).
Wright, I. J. et al. The worldwide leaf economics spectrum. Nature 428, 821–827 (2004).
Ruiz-Jaen, M. C. & Potvin, C. Can we predict carbon stocks in tropical ecosystems from tree diversity? Comparing species and functional diversity in a plantation and a natural forest. New Phytol. 189, 978–987 (2011).
Grubb, P. J. A positive distrust in simplicity-lessons from plant defences and from competition among plants and among animals. J. Ecol. 80, 585–610 (1992).
Hanley, M. E., Lamont, B. B., Fairbanks, M. M. & Rafferty, C. M. Plant structural traits and their role in anti-herbivore defence. Perspect. Plant Ecol. 8, 157–178 (2007).
Burns, K. C. Spinescence in the New Zealand flora: parallels with Australia. N. Z. J. Bot. 54, 273–289 (2016).
Goheen, J. R., Young, T. P., Keesing, F. & Palmer, T. M. Consequences of herbivory by native ungulates for the reproduction of a savanna tree. J. Ecol. 95, 129–138 (2007).
Goldel, B., Kissling, W. D. & Svenning, J.-C. Geographical variation and environmental correlates of functional trait distributions in palms (Arecaceae) across the New World. Bot. J. Linn. Soc. 179, 602–617 (2015).
Alves-Silva, E. & Del-Claro, K. Herbivory causes increases in leaf spinescence and fluctuating asymmetry as a mechanism of delayed induced resistance in a tropical savanna tree. Plant Ecol. Evol. 149, 73–80 (2016).
Cooper, S. M. & Ginnett, T. F. Spines protect plants against browsing by small climbing mammals. Oecologia 113, 219–221 (1998).
Charles-Dominique, T. et al. Spiny plants, mammal browsers, and the origin of African savannas. Proc. Natl Acad. Sci. USA 113, E5572–E5579 (2016).
Ratnam, J., Tomlinson, K. W., Rasquinha, D. N. & Sankaran, M. Savannahs of Asia: antiquity, biogeography, and an uncertain future. Philos. Trans. R. Soc. B. 371, 20150305 (2016).
Scholes, R. & Archer, S. Tree-grass interactions in savannas. Annu. Rev. Ecol. Syst. 28, 517–544 (1997).
Cerling, T. E. Development of grasslands and savannas in East Africa during the Neogene. Palaeogeogr. Palaeoclimatol. Palaeoecol. 97, 241–247 (1992).
Brown, R. W. Additions to the flora of the Green River formation. U. S. Geol. Surv. Prof. Paper, U. S. Gov. Print. Off. 154-J, 279–292 (1929).
Manchester, S. Oligocene fossil plants of the John Day Formation, Oregon. Or. Geol. 49, 115d–127d (1987).
Meyer, H. W. & Manchester, S. R. Oligocene Bridge Creek flora of the John Day Formation, Oregon (Univ. California Press, 1997).
Lancucka-Srodoniowa, M. Tortonian flora from the “Gdow Bay” in the south of Poland. Acta Palaeobot. 7, 1–134 (1966).
Yuan, J. et al. Rapid drift of the Tethyan Himalaya terrane before two-stage India-Asia collision. Natl Sci. Rev. 8, nwaa173 (2021).
Spicer, R. A. et al. Why the ‘Uplift of the Tibetan Plateau’is a myth. Natl Sci. Rev. 8, nwaa091 (2021).
Spicer, R. A. Tibet, the Himalaya, Asian monsoons and biodiversity–In what ways are they related? Plant Divers. 39, 233–244 (2017).
DeCelles, P. G., Kapp, P., Gehrels, G. E. & Ding, L. Paleocene-Eocene foreland basin evolution in the Himalaya of southern Tibet and Nepal: implications for the age of initial India-Asia collision. Tectonics 33, 824–849 (2014).
Royden, L. H., Burchfiel, B. C. & van der Hilst, R. D. The geological evolution of the Tibetan Plateau. Science 321, 1054–1058 (2008).
Deng, T., Wu, F. X., Zhou, Z. K. & Su, T. Tibetan Plateau: an evolutionary junction for the history of modern biodiversity. Sci. China Earth Sci. 63, 172–187 (2020).
Favre, A. et al. The role of the uplift of the Qinghai‐Tibetan Plateau for the evolution of Tibetan biotas. Biol. Rev. 90, 236–253 (2015).
Su, T. et al. A Middle Eocene lowland humid subtropical “Shangri-La” ecosystem in central Tibet. Proc. Natl Acad. Sci. USA 117, 32989–32995 (2020).
Scientific Expedition Team to the Qinghai-Xizang Plateau. Vegetation of Xizang (Tibet) (Sci. Press, 1988).
Liu. X. H. Paleoelevation History and Evolution of the Cenozoic Lunpola basin, Central Tibet. Doctoral thesis (Institute of Tibetan Plateau Research, Chinese Academy of Sciences, 2018).
Xiong, Z. Y. et al. The rise and demise of the Paleogene Central Tibetan Valley. Sci. Adv. 8, eabj0944 (2022).
Reichgelt, T., West, C. K. & Greenwood, D. R. The relation between global palm distribution and climate. Sci. Rep. 8, 4721 (2018).
Farnsworth, A. et al. Paleoclimate model-derived thermal lapse rates: towards increasing precision in paleoaltimetry studies. Earth Planet. Sci. Lett. 564, 116903 (2021).
Spicer, R. A. et al. Why do foliar physiognomic climate estimates sometimes differ from those observed? Insights from taphonomic information loss and a CLAMP case study from the Ganges Delta. Palaeogeogr. Palaeoclimatol. Palaeoecol. 302, 381–395 (2011).
Walter, H. Vegetation of the Earth and Ecological Systems of the Geo-biosphere (Springer Berlin Heidelb., 1973).
Burley, J. Encyclopedia of Forest Sciences (Acad. Press, 2004).
Deng, T. et al. A mammalian fossil from the Dingqing Formation in the Lunpola Basin, northern Tibet, and its relevance to age and paleo-altimetry. Sci. Bull. 57, 261–269 (2012).
Ma, P. F. et al. Late Oligocene-early Miocene evolution of the Lunpola Basin, central Tibetan Plateau, evidences from successive lacustrine records. Gondwana Res. 48, 224–236 (2017).
Hempson, G. P., Archibald, S. & Bond, W. J. A continent-wide assessment of the form and intensity of large mammal herbivory in Africa. Science 350, 1056–1061 (2015).
Spicer, R. A. The formation and interpretation of plant fossil assemblages. Adv. Bot. Res. 16, 95–191 (1989).
Gibson, D. J. Grasses and Grassland Ecology (Oxford Univ. Press, 2009).
Eltringham, S. K. The Hippos: Natural History and Conservation (Princeton Univ. Press, 1999).
Jiang, H. et al. Oligocene Koelreuteria (Sapindaceae) from the Lunpola Basin in central Tibet and its implication for early diversification of the genus. J. Asian Earth Sci. 175, 99–108 (2019).
Liu, J. et al. Biotic interchange through lowlands of Tibetan Plateau suture zones during Paleogene. Palaeogeogr. Palaeoclimatol. Palaeoecol. 524, 33–40 (2019).
Jia, L. B. et al. First fossil record of Cedrelospermum (Ulmaceae) from the Qinghai-Tibetan Plateau: implications for morphological evolution and biogeography. J. Syst. Evol. 57, 94–104 (2019).
Su, T. et al. No high Tibetan Plateau until the Neogene. Sci. Adv. 5, eaav2189 (2019).
Zhang, Y. L., Li, B. Y. & Zheng, D. A discussion on the boundary and area of the Tibetan Plateau in China. Geol. Res. 21, 1–8 (2002).
Yao, T. D. et al. From Tibetan Plateau to Third Pole and Pan-Third Pole. Bull. Chin. Acad. Sci. 32, 924–931 (2017).
Spicer, R. A., Farnsworth, A. & Su, T. Cenozoic topography, monsoons and biodiversity conservation within the Tibetan Region: an evolving story. Plant Divers. 42, 229–254 (2020).
Liu, X. H., Xu, Q. & Ding, L. Differential surface uplift: Cenozoic paleoelevation history of the Tibetan Plateau. Sci. China Earth Sci. 59, 2105–2120 (2016).
Ding, L., Li, Z. Y. & Song, P. P. Core fragments of Tibetan Plateau from Gondwanaland united in Northern Hemisphere. Bull. Chin. Acad. Sci. 32, 945–950 (2017).
Deng, T. & Ding, L. Paleoaltimetry reconstructions of the Tibetan Plateau: progress and contradictions. Natl Sci. Rev. 2, 417–437 (2015).
Li, S. F. et al. Orographic evolution of northern Tibet shaped vegetation and plant diversity in eastern Asia. Sci. Adv. 7, eabc7741 (2021).
Ding, L. et al. The Andean-type Gangdese Mountains: Paleoelevation record from the Paleocene–Eocene Linzhou Basin. Earth Planet. Sci. Lett. 392, 250–264 (2014).
Deng, T. et al. Review: implications of vertebrate fossils for paleo-elevations of the Tibetan Plateau. Glob. Planet. Change 174, 58–69 (2019).
Westerhold, T. et al. An astronomically dated record of Earth’s climate and its predictability over the last 66 million years. Science 369, 1383–1387 (2020).
Nemani, R. R. et al. Climate-driven increases in global terrestrial net primary production from 1982 to 1999. Science 300, 1560–1563 (2003).
Hopkins, W. G. Introduction to Plant Physiology (John Wiley & Sons, 1999).
Sun, J. M., Liu, W. G., Liu, Z. H. & Fu, B. H. Effects of the uplift of the Tibetan Plateau and retreat of Neotethys ocean on the stepwise aridification of mid-latitude Asian interior. Bull. Chin. Acad. Sci. 32, 951–958 (2017).
Zong, G. F. Cenezoic Mammals and Environment of Hengduan Mountains Region (China Ocean Press, 1996).
Deng, T. et al. An Oligocene giant rhino provides insights into Paraceratherium evolution. Commun. Biol. 4, 639 (2021).
Young, T. P., Stanton, M. L. & Christian, C. E. Effects of natural and simulated herbivory on spine lengths of Acacia drepanolobium in Kenya. Oikos 101, 171–179 (2003).
Karban, R. & Myers, J. H. Induced plant responses to herbivory. Annu. Rev. Ecol. Syst. 20, 331–348 (1989).
Huntly, N. Herbivores and the dynamics of communities and ecosystems. Annu. Rev. Ecol. Syst. 22, 477–503 (1991).
Asner, G. P. et al. Large-scale impacts of herbivores on the structural diversity of African savannas. Proc. Natl Acad. Sci. USA 106, 4947–4952 (2009).
Sankaran, M., Augustine, D. J. & Ratnam, J. Native ungulates of diverse body sizes collectively regulate long‐term woody plant demography and structure of a semi‐arid savanna. J. Ecol. 101, 1389–1399 (2013).
Staver, A. C. & Bond, W. J. Is there a ‘browse trap’? Dynamics of herbivore impacts on trees and grasses in an African savanna. J. Ecol. 102, 595–602 (2014).
Bakker, E. S. et al. Combining paleo-data and modern exclosure experiments to assess the impact of megafauna extinctions on woody vegetation. Proc. Natl Acad. Sci. USA 113, 847–855 (2016).
Spicer, R. A. et al. The topographic evolution of the Tibetan Region as revealed by palaeontology. Palaeobio. Palaeoenv. 101, 213–243 (2021).
Rowley, D. B. & Currie, B. S. Palaeo-altimetry of the late Eocene to Miocene Lunpola basin, central Tibet. Nature 439, 677–681 (2006).
Sun, J. M. et al. Palynological evidence for the latest Oligocene-early Miocene paleoelevation estimate in the Lunpola Basin, central Tibet. Palaeogeogr. Palaeoclimatol. Palaeoecol. 399, 21–30 (2014).
DeCelles, P. G., Kapp, P., Ding, L. & Gehrels, G. E. Late Cretaceous to middle Tertiary basin evolution in the central Tibetan Plateau: Changing environments in response to tectonic partitioning, aridification, and regional elevation gain. Geol. Soc. Am. Bull. 119, 654–680 (2007).
Tang, H. et al. Extinct genus Lagokarpos reveals a biogeographic connection between Tibet and other regions in the Northern Hemisphere during the Paleogene. J. Syst. Evol. 57, 670–677 (2019).
Wang, T. X. et al. Fossil fruits of Illigera (Hernandiaceae) from the Eocene of central Tibetan Plateau. J. Syst. Evol. 59, 1276–1286 (2021).
Del Rio, C. et al. Asclepiadospermum gen. nov., the earliest fossil record of Asclepiadoideae (Apocynaceae) from the early Eocene of central Qinghai-Tibetan Plateau, and its biogeographic implications. Am. J. Bot. 107, 126–138 (2020).
Xu, Z. Y. The Tertiary and its petroleum potential in the Lunpola Basin, Tibet. Oil Gas. Geol. 1, 153–158 (1980).
Zhang, K. X. et al. Paleogene-Neogene stratigraphic realm and sedimentary sequence of the Qinghai-Tibet Plateau and their response to uplift of the plateau. Sci. China Earth Sci. 53, 1271–1294 (2010).
Wu, Y. F. & Chen, Y. Y. Fossil cyprinid fishes from the late Tertiary of north Xizang, China. Vertebrata Palasiat. 18, 15–20 (1980).
Wu, F. X., Miao, D. S., Chang, M. M., Shi, G. L. & Wang, N. Fossil climbing perch and associated plant megafossils indicate a warm and wet central Tibet during the late Oligocene. Sci. Rep. 7, 878 (2017).
Cai, C. Y., Huang, D. Y., Wu, F. X., Zhao, M. & Wang, N. Tertiary water striders (Hemiptera, Gerromorpha, Gerridae) from the central Tibetan Plateau and their palaeobiogeographic implications. J. Asian Earth Sci. 175, 121–127 (2017).
Low, S. L. et al. Oligocene Limnobiophyllum (Araceae) from the central Tibetan Plateau and its evolutionary and palaeoenvironmental implications. J. Syst. Palaeontol. 18, 415–431 (2020).
Bell, A. D. & Bryan, A. Plant Form: An Illustrated Guide to Flowering Plant Morphology (Timber Press, 2008).
Zanne, A. E. et al. Three keys to the radiation of angiosperms into freezing environments. Nature 506, 89–92 (2014).
Revell, L. J. phytools: an R package for phylogenetic comparative biology (and other things). Methods Ecol. Evol. 3, 217–223 (2012).
Paradis, E. & Schliep, K. ape 5.0: an environment for modern phylogenetics and evolutionary analyses in R. Bioinformatics. 35, 526–528 (2019).
Harmon, L. J., Weir, J. T., Brock, C. D., Glor, R. E. & Challenger, W. GEIGER: investigating evolutionary radiations. Bioinformatics. 24, 129–131 (2008).
Maddison, W. P. Confounding asymmetries in evolutionary diversification and character change. Evolution 60, 1743–1746 (2006).
Forest, C. E., Molnar, P. & Emanuel, K. A. Palaeoaltimetry from energy conservation principles. Nature 374, 347–350 (1995).
Valdes, P. J. et al. The BRIDGE HadCM3 family of climate models: HadCM3@ Bristol v1.0. Geosci. Model Dev. 10, 3715–3743 (2017).
Gough, D. O. Solar interior structure and luminosity variations. Sol. Phys. 74, 21–34 (1981).
Foster, G. L., Royer, D. L. & Lunt, D. J. Future climate forcing potentially without precedent in the last 420 million years. Nat. Commun. 8, 14845 (2017).
Cox, P. M. Description of the “TRIFFID” Dynamic Global Vegetation Model. 1–16 (Met Office Hadley Centre, 2001).
Cox, P., Huntingford, C. & Harding, R. A canopy conductance and photosynthesis model for use in a GCM land surface scheme. J. Hydrol. 212, 79–94 (1998).
McInerney, F. A., Strömberg, C. A. E. & White, J. W. C. The Neogene transition from C3 to C4 grasslands in North America stable carbon isotope ratios of fossil phytoliths. Paleobiology 37, 23–49 (2011).
Lu, H. Y. et al. Phytoliths as quantitative indicators for the reconstruction of past environmental conditions in China II: palaeoenvironmental reconstruction in the Loess Plateau. Quat. Sci. Rev. 25, 945–959 (2006).
We are grateful to members of the Paleoecology Research Group at Xishuangbanna Tropical Botanical Garden (XTBG) and Institute of Vertebrate Paleontology and Paleoanthropology (IVPP) who participated in numerous fossil collection expeditions on the Tibetan Plateau. We thank Professor Houyuan Lu and Professor Caroline A.E. Strömberg for contributions to the identification of phytoliths; the Central Laboratory of Public Technology Service Center of XTBG for help with photography. This work is supported by National Natural Science Foundation of China (NSFC) (Nos. 41988101 and 41922010), the Second Tibetan Plateau Scientific Expedition programme (No. 2019QZKK0705), Natural Environment Research Council of the UK (NERC) (Nos. 41661134049 and NE/P013805/1), the Strategic Priority Research Program of the Chinese Academy of Sciences (CAS) (Nos. XDA20070301 and XDB26000000), Youth Innovation Promotion Association, CAS (No. Y2021105), and the West Light Foundation, CAS (No. 2020000023).
The authors declare no competing interests.
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Zhang, X., Gélin, U., Spicer, R.A. et al. Rapid Eocene diversification of spiny plants in subtropical woodlands of central Tibet. Nat Commun 13, 3787 (2022). https://doi.org/10.1038/s41467-022-31512-z