The State of the Climate Report for 2014 presents a summary of temperature, rainfall, tropical cyclone, sea level and greenhouse gas concentration observations over recent years.


The warming trend occurs against a background of year-to-year climate variability, mostly associated with El Niño and La Niña in the tropical Pacific. 2013 was Australia’s warmest year on record, being 1.2°C above the 1961–1990 average of 21.8°C and 0.17°C above the previous warmest year in 2005. Seven of the ten warmest years on record have occurred since 1998.

Australia’s climate has warmed since national records began in 1910, especially since 1950. Mean surface air temperature has warmed by 0.9°C since 1910. Daytime maximum temperatures have warmed by 0.8°C over the same period, while overnight minimum temperatures have warmed by 1.1°C.

Anomalies are the departures from the 1961–1990 average climatological period. Sea-surface temperature values are provided for a region around Australia (from 4°S to 46°S and from 94°E to 174°E).

Time series of anomalies in sea-surface temperature and temperature over land in the Australian region.  ©Bureau of Meteorology

Sea-surface temperatures in the Australian region have warmed by 0.9°C since 1900. In 2013, temperatures were 0.5°C above the 1961–1990 average of 22.3°C. Sea-surface temperatures around parts of Australia have been mostly well-above average since 2010, with persistent regions of very warm to highest-on-record temperatures to the south and west of the continent throughout much of 2013.

Since 2001, the number of extreme heat records in Australia has outnumbered extreme cool records by almost 3 to 1 for daytime maximum temperatures, and almost 5 to 1 for night-time minimum temperatures.


Distribution of monthly maximum temperature (left) and monthly minimum temperature (right), expressed as anomalies (standardised), aggregated across 104 locations and all months of the year, for three periods: 1951–1980 (pink, grey), 1981–2010 (orange, green) and 1999–2013 (red, blue). Means and standard deviations used in the calculation of the standardised anomalies are with respect to the 1951–1980 base period in each case. Very warm and very cool months correspond to two standard deviations or more from the mean. The vertical axis shows how often temperature anomalies of various sizes have occurred in the indicated periods.

Distribution of monthly maximum temperature (left) and monthly minimum temperature  ©Bureau of Meteorology

Very warm months that occurred just over 2 per cent of the time during the period 1951 to 1980 occurred nearly 7 per cent of the time during 1981 to 2010, and around 10 per cent of the time over the past 15 years. At the same time the frequency of very cool months has declined by around a third since the earlier period.


Australian rainfall is highly variable, which makes it difficult to identify significant trends over time, nevertheless some rainfall changes are discernible.

Australian average annual rainfall has increased since national records began in 1900, largely due to increases in rainfall from October to April, and most markedly across the northwest.

Southern Australia typically receives most of its rainfall during the cooler months of the year. In recent decades declines in rainfall have been observed in the southwest and in the southeast of the continent.


Southern wet season (April–November) rainfall deciles since 1996. A decile map shows the extent that rainfall is above average, average or below average for the specified period, in comparison with the entire rainfall record from 1900. The southern wet season is defined as April to November by the Bureau of Meteorology.

Southern wet season rainfall deciles  ©Bureau of Meteorology

Since 1970 there has been a 17 per cent decline in average winter rainfall in the southwest of Australia. The southeast has experienced a 15 per cent decline in late autumn and early winter rainfall since the mid-1990s, with a 25 per cent reduction in average rainfall across April and May. Declining rainfall in the southwest has been statistically significant over the recent period, and has occurred as a series of step changes. The decline in this region has also been characterised by a lack of very wet winters.

The cool season drying over southern Australia in recent decades, and evidence of increased rainfall over the Southern Ocean, is associated with changes in atmospheric circulation. While natural variability likely plays a role, a range of studies suggest ozone depletion and global warming are contributing to circulation and pressure changes, most clearly impacting on the southwest. Uncertainties remain, and this is an area of ongoing research.

The reduction in rainfall is amplified in streamflow in our rivers and streams. In the far southwest, streamflow has declined by more than 50 percent since the mid-1970s. In the far southeast, streamflow during the 1997–2009 Millennium Drought was around half the long-term average.

The duration, frequency and intensity of heatwaves have increased across many parts of Australia, based on daily temperature records since 1950 when coverage is sufficient for heatwave analysis. Days where extreme heat is widespread across the continent have become more common in the past twenty years.

Some recent instances of extreme summer temperatures experienced around the world, including record-breaking summer temperatures in Australia over 2012–2013, are very unlikely to have been caused by natural variability alone.

Fire activity is sensitive to many different factors; the meteorological factors include wind speed, humidity, temperature and drought. Fire weather is monitored in Australia with the Forest Fire Danger Index (FFDI). Annual cumulative FFDI, which represents the occurrence and severity of daily fire weather across the year, increased with statistical significance at 16 of 38 climate reference sites from 1973–2010, with non-statistically significant increases at the other sites. Extreme fire-weather days have become more extreme at 24 of the 38 locations since the 1970s.

The number of significant increases is greatest in the southeast, while the largest increases in the index occurred inland rather than near the coast. The largest increases in seasonal FFDI occurred during spring and autumn, while summer had the fewest significant trends. This indicates a lengthened fire season.

Heavy Rainfall

Natural variability continues to play the dominant role in extreme rainfall in Australia. Observational data show that the area of the continent receiving very high rainfall totals (above the 90th percentile) on seasonal and annual timescales has increased since the mid-twentieth century, however few statistically significant trends in changing rainfall intensity have been found across the continent.

Recent studies examining heavy monthly to seasonal rainfall events that occurred in eastern Australia between 2010 and 2012 have shown that the magnitude of extreme rainfall is mostly explained by natural variability, with potentially a small additional contribution from global warming. Understanding changes to Australian rainfall intensity is an area of ongoing research.

Tropical cyclones

It is difficult to draw conclusions regarding changes in the frequency and intensity of tropical cyclones in the Australian region because of the shortness of the satellite record, changes in historical methods of analysis, and the high variability in tropical cyclone numbers. The research on cyclone frequency in the Australian region is equivocal, with some studies suggesting no change and others a decrease in numbers since the 1970s.

Global Atmosphere and Cryosphere

Warming in Australia is consistent with warming observed across the globe in recent decades. Evidence that the Earth’s climate continues to warm is unequivocal. Multiple lines of evidence indicate that it is extremely likely that the dominant cause of recent warming is humaninduced greenhouse gas emissions and not natural climate variability.

Much of the observed warming has occurred since the 1950s. There has been warming at the Earth’s surface, warming in the lower and middle atmosphere (troposphere), warming of sea-surface temperatures and warming below the ocean surface. Global warming is also apparent from decreases in the mass of Greenland and Antarctic ice sheets (ice attached to land), net decrease in glacier volumes, large reductions in Arctic sea-ice extent, higher global sea level and reductions in snow cover. 

The instrumental record shows that global mean temperature has risen by 0.85°C (± 0.2°C) since 1880. All of the warmest 20 years on record have occurred since 1990.

Ice-mass loss from Antarctic and Greenland ice sheets has accelerated. The mean estimated rate of ice loss from the Antarctic ice sheet has increased nearly five-fold from an estimated mean of 30 gigatonnes per year (Gt/yr) for the period from 1992 to 2001, to 147 Gt/yr for the period 2002 to 2011. The rate of ice loss from the Greenland ice sheet has increased from 34 to 215 Gt/yr over the same period.

The average rate of ice loss from glaciers around the world, excluding glaciers on the periphery of the ice sheets, was very likely 226 Gt/yr over the period 1971 to 2009, and very likely 275 Gt/yr over the period 1993 to 2009.

Arctic summer minimum sea-ice extent has declined by between 9.4 and 13.6 per cent per decade since 1979, a rate that is likely unprecedented in at least the past 1,450 years.

Antarctic annual-mean total seaice extent has slightly increased by 1.2 per cent to 1.8 per cent per decade since 1979. This net increase represents the sum of contrasting regional trends around Antarctica.

The overall increase in Antarctic seaice extent has been linked to several possible drivers, including freshening of surface waters due to increased precipitation and the enhanced melting of ice shelves, and changes in atmospheric circulation resulting in greater sea-ice dispersion.

Ocean heat content

Warming of the world’s oceans accounts for more than 90 per cent of additional energy accumulated from the enhanced greenhouse effect, making this one of the most important measures for monitoring and understanding climate change.

The ocean today is warmer, and sea levels higher, than at any time since the instrumental record began.

Ocean heat content is a key indicator of heat accumulated in the oceans, and is measured in units of energy known as joules. The upper layer of the ocean, from the surface to a depth of 700 metres, has increased its heat content by around 17x1022 joules since 1971, accounting for around 63 per cent of additional energy accumulated by the climate system. Warming below 700metres over the same period accounts for approximately 30 per cent of additional energy. The remaining 7 per cent has been added to the cryosphere, atmosphere and land surface.

Sea level

Global mean sea level has increased throughout the 20th century. By 2012 sea level was 225 mm (± 30 mm) higher than in 1880, the earliest year for which robust estimates are available.

The largest contributions to global sea-level rise have been thermal expansion of the oceans (expansion through warming) and the loss of mass from glaciers and ice sheets.


High-quality global sea-level measurements from satellite altimetry since the start of 1993 (orange line), in addition to the longer-term records from tide gauges (green line, with shading providing an indication of the confidence range of the estimate).

Inset: Sea-level increase since 1993 from the satellite altimetry. The light green line shows the monthly data, the dark green line the three-month moving average, and the orange line the linear trend.

Global sea-level measurements  ©Bureau of Meteorology

Rates of sea-level rise vary around the Australian region, with higher sea-level rise observed in the north and rates similar to the global average observed in the south and east. Global sea level fell during the intense La Niña event of 2010–2011. This was ascribed partly to the exceptionally high rainfall over land which resulted in floods in Australia, northern South America, and Southeast Asia. This was compounded by the long residence time of water over inland Australia. Recent observations show that sea levels have rebounded in line with the long-term trend.

Ocean acidification

Ocean acidification is caused by the ocean absorbing higher levels of carbon dioxide (CO2) from the atmosphere, and is therefore another consequence of the accumulation of anthropogenic CO2 in the Earth’s climate system. Ocean acidity is measured in units of ‘pH’. A lowering pH means increasing acidity. The pH of surface waters in the open ocean has decreased by about 0.1 since 1750, equivalent to a 26 per cent increase in the activity of hydrogen ions (a measure of ocean acidity).

Carbon dioxide emissions

Global anthropogenic CO2 emissions into the atmosphere in 2013 are estimated to be 38.8 billion tonnes of CO2 (10.6 billion tonnes of carbon), the highest in history and about 46 per cent higher than in 1990. Global CO2 emissions from the use of fossil fuel are estimated to have increased in 2013 by 2.1 per cent compared with the average of 3.1 per cent per year from 2000 to 2012.


Graphs showing sources and sinks of carbon dioxide

Most of the CO2 emissions from human activities are from fossil-fuel combustion and land-use change (top graph). Emissions are expressed in gigatonnes of carbon (C) per year. A gigatonne is equal to 1 billion tonnes. One tonne of carbon (C) equals 3.67 tonnes of carbon dioxide (CO2). CO2 emissions from human activities have been taken up by the ocean (middle graph, in blue, where negative values are uptake), by land vegetation (middle graph, in gold), or remain in the atmosphere. There has been an increase in the atmospheric concentration of CO2 (bottom graph, in red), as identified by the trend in the ratio of different types (isotopes) of carbon in atmospheric CO2 (bottom graph, in black, from the year 1000). CO2 and the carbon-13 isotope ratio in CO2 (δ13C) are measured from air in Antarctic ice and form (compacted snow) samples from the Australian Antarctic Science Program, and at Cape Grim (northwest Tasmania).

Sources and sinks of carbon dioxide  ©Bureau of Meteorology

Since the industrial revolution more than two centuries ago, about 30 per cent of the anthropogenic CO2 emissions have been taken up by the ocean and about 30 per cent by land vegetation. The remaining 40 per cent of emissions have led to an increase in the concentration of CO2 in the atmosphere.

The origin of CO2 in the atmosphere can be determined by examining the different types (isotopes) of carbon in air samples. This identifies the additional CO2 as coming from human activities, mainly the burning of fossil fuel, and not from natural sources.

Greenhouse gas concentrations

Atmospheric concentrations of major greenhouse gases, including CO2, methane (CH4), nitrous oxide (N2O), and a group of synthetic greenhouse gases, are increasing.

Atmospheric greenhouse gas levels have exceeded the record levels reported in the State of the Climate 2012 report, continuing the increase observed over the past century. The global mean CO2 level in 2013 was 395 parts per million (ppm) — a 43 per cent increase from pre-industrial (1750) concentrations, and likely the highest level in at least 2 million years.

The global CO2 annual increase from 2012 to 2013 was 2.5 ppm, and the increase of 5.1 ppm since 2011 is the largest two-year increase observed in the historical record. Global atmospheric CH4 concentration is 151 per cent higher, and N2O 21 per cent higher than in 1750, and they are at their highest levels for at least 800 000 years.

The impact of all greenhouse gases in the atmosphere combined can be expressed as an ‘equivalent CO2’ atmospheric concentration, which reached 480 ppm in 2013.


Global mean greenhouse gas concentrations (‘ppm’ is parts per million, while ‘ppb’ is parts per billion) determined from continuous monitoring by CSIRO, the Bureau of Meteorology and the CSIRO/Advanced Global Atmospheric Gases Experiment at Cape Grim since 1976, in Antarctic firn air samples since the mid-1970s, and globally by CSIRO since the mid-1980s.

Global mean greenhouse gas concentrations  ©Bureau of Meteorology

Future climate scenarios for Australia

Australian temperatures are projected to continue to warm, rising by 0.6 to 1.5°C by 2030 compared with the climate of 1980 to 1999; noting that 1910 to 1990 warmed by 0.6°C. Warming by 2070, compared to 1980 to 1999, is projected to be 1.0 to 2.5°C for low greenhouse gas emissions and 2.2 to 5.0°C for high emissions. The high-emissions scenario assumes a continuation into the future of the global CO2 emissions growth seen over the past decade, whereas the low-emissions scenario assumes a significant reduction in global emissions over the coming decades. These projected changes in temperature will be felt through an increase in the number of hot days and warm nights and a decline in cool days and cold nights.

Further decreases in average rainfall are expected over southern Australia compared with the climate of 1980 to 1999: a zero to 20 per cent decrease by 2070 for low emissions; and a 30 per cent decrease to 5 per cent increase by 2070 for high emissions, with largest decreases in winter and spring. For northern Australia the projected changes in rainfall range from a 20 per cent decrease to 10 per cent increase by 2070 for low emissions, and a 30 per cent decrease to 20 per cent increase for high emissions. Droughts are expected to become more frequent and severe in southern Australia.

An increase in the number and intensity of extreme rainfall events is projected for most regions.The number of extreme fire-weather days is projected to grow in southern and eastern Australia; by 10 to 50 per cent for low emissions and 100 to 300 per cent for high emissions, by 2050 compared with the climate of 1980 to 1999.

Fewer tropical cyclones are projected for the Australian region, on average, with an increased proportion of intense cyclones. However, confidence in tropical cyclone projections is low.

Sea-level rise around the Australian coastline by 2100 is likely to be similar to the projected global rise of 0.28 to 0.61 metres for low emissions and 0.52 to 0.98 metres for high emissions, relative to 1986–2005. Higher sea levels by 2100 are possible if there is a collapse of sectors of the Antarctic ice sheet grounded below sea level. There is medium confidence that such an additional rise would not exceed several tenths of a metre by 2100. Under all scenarios, sea level will continue to rise after 2100, with high emissions leading to a sea-level rise of 1 metre to more than 3 metres by 2300. Increases in mean sea level will increase the frequency of extreme se a-level events.

Ocean-acidity levels will continue to increase as the ocean absorbs anthropogenic carbon-dioxide emissions.

Reductions in global greenhouse gas emissions would increase the chance of constraining future global warming. Nonetheless adaptation is required because some warming and associated changes are unavoidable.

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