1. Introduction
Precipitation is a critical component of the climate system; it intertwines the energy budget and the water cycle via its link to latent heat flux (Stephens et al. 2012), impacts upon society (by causation of flooding, famine, and freshwater availability), and is expected to increase globally with warming of Earth, particularly within regions of moisture convergence (Allan et al. 2020). Precipitation is one of the most challenging variables to represent in simulations since they must capture its high spatiotemporal variability, which is determined by multiple factors including longwave and shortwave radiation, convection, humidity, and precipitation microphysics (Tapiador et al. 2019). Climate models have struggled with accurately representing precipitation, with precipitation occurring too often, too lightly (Chen et al. 1996; Stephens et al. 2010; Trenberth et al. 2017), and too early in the day (Dai et al. 1999; Dai and Trenberth 2004; Dai 2006; Trenberth et al. 2003; DeMott et al. 2007). Evaluating and addressing long-standing and systematic errors in the diurnal cycle of precipitation are central to improving the realism of the models used to make future climate projections (Eyring et al. 2016).
Observational studies have determined key features of the diurnal cycle across the globe: the diurnal cycle is stronger over land than over ocean, with precipitation typically peaking from midafternoon to evening over land and in the morning over the ocean (Janowiak et al. 1994; Dai 2001, 2006; Dai and Trenberth 2004; Dai et al. 2007; Yang and Slingo 2001; Nesbitt and Zipser 2003; Liu and Zipser 2008; Kikuchi and Wang 2008; Kidd et al. 2013; Covey et al. 2016; Watters and Battaglia 2019; Battaglia et al. 2020a; Minobe et al. 2020). Furthermore, the diurnal amplitude over land is stronger in summer than in winter (Wallace 1975; Dai et al. 1999, 2007; Dai 2006; Yang and Slingo 2001; Kikuchi and Wang 2008; Watters and Battaglia 2019; Battaglia et al. 2020a), and the diurnal cycle of precipitation accumulation is driven by its occurrence instead of its intensity (Dai et al. 1999, 2007; Watters and Battaglia 2019). Some studies have identified that weather and climate models simulate the time of maximum earlier than observed (Yang and Slingo 2001; Betts and Jakob 2002; Trenberth et al. 2003; Dai and Trenberth 2004; Dai 2006; Dirmeyer et al. 2012; Kidd et al. 2013; Flato et al. 2014; Rosa and Collins 2013; Covey et al. 2016). In convection-parameterized coupled climate models, this early diurnal peak in warm-season precipitation over land may be related to the premature onset of cumulus convection, while their weak diurnal oceanic amplitudes may be related to a lack of diurnal variations in their simulated sea surface temperatures (Dai and Trenberth 2004). Convection-permitting models appear to better represent diurnal phase than convection-parameterized models (Dirmeyer et al. 2012; Scaff et al. 2020), with some skill in capturing nocturnal precipitation peaks in mountainous regions, though they tend to overestimate mean precipitation and diurnal amplitude (Dirmeyer et al. 2012). Furthermore, turning off the parameterized convection scheme is central to improving the diurnal cycle representation rather than increasing horizontal resolution (Pearson et al. 2014). Some studies have evaluated the performance of the preceding phases of CMIP global climate models, with CMIP3 and CMIP5 simulations of diurnal precipitation amplitudes generally identified to be realistic, while their precipitation typically peaks several hours earlier than surface and satellite observations (Dai 2006; Randall et al. 2007; Rosa and Collins 2013; Flato et al. 2014; Covey et al. 2016). The latest CMIP6 multidecade model simulations are yet to be analyzed.
Satellite constellations are capable of observing the diurnal cycle of precipitation across the globe, due to their consistent coverage, fine spatiotemporal sampling, and access to remote areas. Global-gridded products generated from passive microwave (PMW) radiometers and infrared (IR) sensors, with calibration to spaceborne radar and ground-based gauges, are commonly used in global diurnal cycle assessments (e.g., Dai 2006; Dai et al. 2007; Covey et al. 2016; Watters and Battaglia 2019; Battaglia et al. 2020a, etc.), including: the Tropical Rainfall Measuring Mission (TRMM) Multisatellite Precipitation Analysis (TMPA/3B42; Huffman et al. 2007), and the successor Global Precipitation Measurement (GPM) mission’s Integrated Multisatellite Retrievals for GPM (IMERG; Huffman et al. 2019b). IMERG advances upon TMPA by providing extended spatial coverage [IMERG: 90°N–S (partial coverage for 60°–90°N/S); TMPA: 50°N–S] at finer spatiotemporal resolution (IMERG: 0.1° × 0.1°, half-hourly; TMPA: 0.25° × 0.25°, 3-hourly), and now incorporates measurements from the TRMM era to provide a 20-yr+ record of precipitation.
The present study evaluates the diurnal cycle of precipitation accumulation for boreal summer from the state-of-the-art IMERG observation, CMIP6 (NCAR and CNRM) model and ECMWF Reanalysis (ERA5; Hersbach et al. 2020) products. Novelties for a global precipitation diurnal cycle study include: the first multidecade analysis with IMERG; the first multidecade evaluation of CMIP6’s NCAR and CNRM models and their different simulations; the first global evaluation of ERA5; the first model and reanalysis assessment at the hourly scale; and the first interannual variability investigation. IMERG’s capability to reliably represent the diurnal cycle has been demonstrated (Watters and Battaglia 2019; Sungmin and Kirstetter 2018; Tan et al. 2019a; Dezfuli et al. 2017; Tang et al. 2020) and is considered to be a global reference in this study. First, the diurnal cycle from IMERG, NCAR, CNRM, and ERA5 over the conterminous United States (CONUS) and the Gulf Stream is analyzed and validated against the regional reference Multi-Radar Multi-Sensor (MRMS) gauge-adjusted ground-based radar network product; MRMS’s radars provide direct near-surface precipitation estimates unlike IMERG’s PMW and IR sensors, though are limited to CONUS coverage only. The capability of the GPM Core Observatory’s (CO) Dual-Frequency Precipitation Radar (DPR) in capturing the diurnal cycle evolution over CONUS is also investigated. Second, IMERG, NCAR, CNRM, and ERA5 representation of diurnal precipitation mean, normalized amplitude, and time of maximum across the globe are compared. The interannual variability of these diurnal precipitation parameters is investigated.
2. Data
The products assessed in this diurnal cycle study are listed in Table 1.
List of data products used for the diurnal cycle analysis. For the CMIP6 models, only one simulation variant is used: r1i1p1f2 for the CNRM simulations, r10i1p1f1 for the NCAR-CESM2 AMIP simulation, and r11i1p1f1 for the NCAR-CESM2 Historical simulation.
a. Observations
1) IMERG
IMERG is the flagship product of the NASA–JAXA GPM mission (Hou et al. 2014; Skofronick-Jackson et al. 2017; Kidd et al. 2020; Watters and Battaglia 2020a). The IMERG algorithm intercalibrates, merges, and interpolates precipitation estimates from the GPM satellite constellation of PMW radiometers in low-Earth orbits, with integration of estimates from geostationary spaceborne IR sensors in PMW-sparse regions, to produce a global-gridded product at 0.1° and 30-min resolution (Huffman et al. 2019b, 2020b). The PMW precipitation estimates (Kummerow et al. 2015; Kidd 2019) are seasonally calibrated to the constellation-reference GPM-CO combined radar and PMW radiometer (CORRA) estimates (Olson 2018; Skofronick-Jackson et al. 2018); further climatological calibration to the Global Precipitation Climatology Project (GPCP), version 2.3, monthly satellite-gauge estimates (Adler et al. 2018) is applied where CORRA is biased (low over high-latitude oceans and high over tropical and midlatitude land; Huffman et al. 2020a). The algorithm enhances PMW coverage by propagating precipitation features using a quasi-Lagrangian interpolation scheme (known as morphing; Tan et al. 2019b; Joyce and Xie 2011), before integrating PMW-calibrated IR precipitation estimates (Hong et al. 2004) into PMW-sparse regions between 60°N and 60°S. This study uses IMERG V06B Final Run precipitationCal data, where the PMW-IR estimates are calibrated to monthly Global Precipitation Climatology Centre (GPCC) gauge analyses (Schneider et al. 2014) over land. IMERG V06B now extends back from the GPM era (from June 2014 to the present) into the TRMM era (from June 2000 to May 2014), in which the TRMM satellite’s radar and radiometer (Simpson et al. 1996; Kummerow et al. 1998) are the constellation reference; the advancements of the GPM-CO beyond the TRMM satellite (including midlatitude coverage, dual-frequency radar, etc.) are described by Iguchi et al. (2018).
This study uses IMERG as a global reference for the diurnal cycle due to its climatological/monthly calibration to gauge-based products (GPCP, GPCC; reducing biases in diurnal precipitation means), use of the intercalibrated GPM constellation (Berg et al. 2016), and skill in capturing the diurnal cycle over CONUS (Sungmin and Kirstetter 2018; Tan et al. 2019b), Africa (Dezfuli et al. 2017), and China (Tang et al. 2020). IMERG tends to observe the time of maximum precipitation less than 1 h after MRMS over central and southeastern CONUS (due to PMW sensors measuring hydrometeors at the ice-scattering level; Tan et al. 2019a), and better captures the African diurnal cycle compared to commonly used, model-evaluator TMPA (Dezfuli et al. 2017; Kidd et al. 2013; Covey et al. 2016). Furthermore, IMERG captures the time of maximum, diurnal precipitation range and diurnal standard deviation from rain gauges across China, unlike ERA5 (Tang et al. 2020). However, IMERG is not without bias, with diurnal amplitudes overestimated over central CONUS (Sungmin and Kirstetter 2018) and underestimated over mountainous regions and southeastern CONUS (Sungmin and Kirstetter 2018; Tan et al. 2019a); furthermore, IMERG observes diurnal phase earlier than MRMS for dissipating mesoscale convective systems (MCSs), due to the heightened sensitivity of IMERG’s PMW sensors to their convective regions (Sungmin and Kirstetter 2018). Further IMERG biases include systematic overestimation of drizzle and underestimation of heavy/convective precipitation (Tan et al. 2016; Kirstetter et al. 2020; Maranan et al. 2020), underestimation in mountainous regions (Ramsauer et al. 2018; Navarro et al. 2019; Tapiador et al. 2020) and of snowfall (Tang et al. 2020), and poor performance in coastal regions (Navarro et al. 2019; Tapiador et al. 2020). Southern Ocean anomalies have also been identified (45°–60°S; Watters and Battaglia 2019, 2020b). IMERG performance can also differ by satellite source (Tan et al. 2016), as PMW radiometers are sensitive to precipitation in the column (Watters and Battaglia 2020a), unlike IR sensors, which can only sense the cloud top. While IR retrievals have less skill in representing precipitation than PMW retrievals (with systematic IR underestimates across most precipitation regimes; Kirstetter et al. 2020; Petersen et al. 2020), their contribution to IMERG is less than for predecessor TMPA due to its inclusion of a PMW morphing scheme (Tan et al. 2019b). IMERG’s morphing scheme and enhanced PMW contribution have also resulted in reduced lags in the time of maximum surface precipitation over CONUS compared to TMPA (Tan et al. 2019a), which along with other PMW-IR products have lagged surface precipitation by a few hours due to each sensor’s measurements aloft (Dai et al. 2007).
2) GPM DPR
The DPR instrument on board the GPM-CO is the only precipitation radar currently in space (Iguchi 2020). It measures the three-dimensional structure of precipitation at Ku- and Ka-band frequencies, with a footprint diameter of 5 km at nadir from an altitude of 407 km and a vertical resolution of 250 m. The Ku-band measurements cover a swath of 245 km centered on the satellite ground track, whereas the Ka-band measurements coincidentally cover the central 120-km region; the Ka-band swath was extended to 245 km on 21 May 2018 (Iguchi et al. 2018; Iguchi 2020). Only precipitation estimates from the central 120-km swath, where coincident Ku- and Ka-band measurements are continuously available, are used in this study. The GPM-CO’s sun-asynchronous orbit enables DPR precipitation estimates throughout all local times.
This study uses the DPR V06A product’s estimated surface precipitation rate (precipRateESurface), produced using the dual-frequency retrieval. This retrieval converts the range-resolved Ku-band and Ka-band received power into measured radar reflectivity factors, corrects for the signal attenuation due to clouds, and applies assumptions on the precipitation size distribution to determine precipitation rates (Iguchi et al. 2018; Iguchi 2020); coincident measurements at two different frequencies enables better constraint of the precipitation size distribution, which in turn improves the precipitation retrieval.
3) MRMS
The MRMS system provides high spatiotemporal (0.01° and 2 min) quantitative precipitation estimate (QPE) and severe weather products over CONUS and southern Canada (Zhang et al. 2016). MRMS is underpinned by ground-based measurements from 146 U.S. S-band dual-polarization Weather Surveillance Radar-1988 Doppler (WSR-88D) instruments and 30 Canadian C-band single-polarization Environment Canada radars. These radar measurements are combined with data from 7000 rain gauges for QPE bias correction (except for snowfall), with inputs from hourly model analyses to aid in quality control of the radar measurements and precipitation-type identification (rain, snow, and hail). The gauge measurements are also subject to quality control. QPEs are typically produced by extrapolating the lowest elevation radar reflectivity factor measurement to the ground, determining the surface precipitation type, and then applying the reflectivity-to-precipitation conversion for the respective precipitation type. This study uses the hourly radar V11 product with local gauge bias correction (GaugeCorr_QPE_01H).
b. CMIP6’s NCAR and CNRM models
CMIP6 models with hourly resolution are chosen for this analysis including: the Second Generation Earth System Model (CNRM-ESM2.1), the coupled Climate Model (CNRM-CM6.1) and its high-resolution counterpart (CNRM-CM6.1-HR) from CNRM-CERFACS, and NCAR’s version-2 Community Earth System Model (NCAR-CESM2). Atmospheric Model Intercomparison Project (AMIP) and Historical simulations are analyzed; AMIP is an atmosphere-only simulation from 1979 with the ocean constrained by observed sea surface temperatures (SST) and sea ice concentrations (SIC; Eyring et al. 2016), and Historical is a coupled atmosphere–ocean simulation starting from 1850 (preindustrial). Because of their prescribed SST and SIC observations, AMIP simulations can approximately capture large-scale circulation system positions (which follow SST patterns) and represent El Niño and La Niña event timings, unlike Historical simulations. Both simulation types include observed historical forcings and prescribed CO2 concentrations. Only NCAR and CNRM models are selected for this analysis, because they were the only models that performed hourly AMIP simulations at the time of analysis; available coupled and high-resolution hourly simulations from these models are also assessed. The CMIP6 models each include different physical components (WCRP 2020b) and have different spatial resolutions.
Representation of the diurnal cycle of precipitation is determined by each model’s convective parameterization scheme (Table 1). NCAR-CESM2’s atmospheric model parameterizes deep convection with a plume ensemble approach, where a conditionally unstable lower troposphere results in an ensemble of updrafts and downdrafts; moist convection occurs in the presence of convective available potential energy (CAPE; UCAR 2020). CNRM-CM6.1 parameterizes dry, shallow, and deep convection using a bulk mass flux scheme, with closure dependent upon a dilute CAPE relaxation (Voldoire et al. 2019; WCRP 2020a). CNRM-ESM2.1 employs the same convective parameterization scheme as CNRM-CM6.1, and only differs by including atmospheric chemistry, aerosols, and the carbon cycle (Séférian et al. 2019).
c. ERA5 reanalysis
The ERA5 global reanalysis (Hersbach et al. 2020) combines observations and models via 4D-Var data assimilation to provide a consistent record of the atmosphere, land, and ocean surfaces from 1979. Observations are assimilated in 12-h windows (0900–2100 UTC, and 2100–0900 UTC) within ECMWF’s Integrated Forecasting System (IFS) Cy41r2, with the atmosphere coupled to land and ocean. A land data assimilation system is weakly coupled with this incremental 4D-Var; daily sea surface temperature and sea ice concentration observations are also included. The IFS parameterizes deep, shallow, and midlevel convection using a bulk mass flux scheme, in which a pair of entraining and detraining plumes represent clouds within the grid box (ECMWF 2020). ERA5 assimilates 6-hourly precipitation estimates over CONUS from the National Centers for Environmental Prediction Stage IV radar-gauge product since 2009 (Lopez 2011; Hersbach et al. 2020). Brightness temperatures from GPM/TRMM PMW constellation members are also assimilated due to their sensitivity to precipitation and atmospheric humidity, though precipitation retrievals from these members are not assimilated.
ERA5 has finer spatiotemporal resolution (31 km and hourly) than its predecessor, ERA-Interim, for capturing weather systems, and improved representation of global precipitation compared to GPCP. Furthermore, the diurnal cycle of convection is improved due to changes to the closure of CAPE (Bechtold et al. 2014), such that land-based precipitation now maximizes in the late afternoon rather than midday (Hersbach et al. 2020). This analysis uses the surface mean total precipitation rate (mtpr) from ERA5, which includes rain and snow generated from the IFS cloud (coarser-than-pixel scale) and convection (subpixel scale) schemes (Hersbach et al. 2018).
3. Method
June–August (JJA) hourly precipitation data are analyzed, as diurnal variations are stronger over Northern Hemisphere land in boreal summer. Coincident JJAs across the range of selected CMIP6 simulations (1979–2008) are evaluated against the full IMERG JJA record (2000–19), and ERA5 is subsampled to the IMERG period. The respective multidecade periods are used to maximize signal to noise and provide relatively consistent results with the coincident 2000–08 period across all products (Fig. S1 in the online supplemental material). The DPR and MRMS products are only available from 2014 and 2015, respectively. Only data from 60°N to 60°S are used for consistency, because IMERG coverage between 60° and 90°N/S is incomplete over snowy/icy surfaces where PMW estimates are unreliable (Huffman et al. 2019b). DPR data are gridded to 1° × 1°.
The interannual variability (IAV) of the diurnal parameters from IMERG, NCAR, CNRM, and ERA5 is assessed and defined as the ratio of the standard deviation of the yearly parameters to the mean of the yearly parameters for diurnal precipitation mean and normalized amplitude—the standard deviation of the yearly parameters for the time of maximum. The cyclical nature of daily time (0000 LST = “2400” LST, i.e., 0000 LST of the next day) is accounted for when determining the IAV of the time of maximum. This is done by converting the time for each year to angles on a unit circle, computing the mean of each angle’s Cartesian coordinates before converting back to a mean time (Jammalamadaka and SenGupta 1999); the standard deviation relative to this mean time is calculated using the minimum time difference between each yearly time and the mean time.
4. CONUS evaluation of the observed and the simulated diurnal cycle of precipitation
Evaluation of the diurnal cycle over CONUS and the Gulf Stream provides novel understanding of the differences between IMERG, NCAR, CNRM, and ERA5. Assessing the diurnal cycle where NCAR, CNRM, and ERA5 coincidentally simulate convection (i.e., mean vertical updrafts at 500 hPa) allows discrepancies with IMERG to be pinpointed to issues in the model’s convection scheme (rather than mismatches in precipitation location); the Rocky Mountains and the Gulf Stream are two regions where ERA5, NCAR, and CNRM all simulate convection (Fig. 1a, regions 1 and 5). Furthermore, MRMS’s gauge-adjusted ground-based radar observations provide a regional reference over CONUS. The MRMS regional reference supersedes the IMERG global reference in this analysis as radars directly sense the vertical structure of precipitation (Battaglia et al. 2020b), observing it close to the ground unlike IMERG’s PMW and IR measurements (Watters and Battaglia 2020a); however, MRMS is restricted to CONUS coverage only, while IMERG provides global coverage with regular updates. Over CONUS, MRMS is used to further validate the diurnal cycle from IMERG, beyond previous studies (Sungmin and Kirstetter 2018; Tan et al. 2019a) by using more years of boreal summer estimates (IMERG: 20 years; MRMS: 6 years). This analysis also assesses the ability of the spaceborne GPM-CO’s radar (DPR) to capture the diurnal cycle of precipitation over CONUS for the first time; the DPR is limited to only seven boreal summers of low-Earth-orbit sampling at present, preventing its use in assessing NCAR, CNRM, and ERA5 at fine scales globally.
The diurnal cycle of precipitation for boreal summer over CONUS and the Gulf Stream: CONUS map plots of (a) average vertical velocity at 500 hPa from ERA5 (negative values represent updrafts) and (b) local solar time of maximum precipitation amount from IMERG, as in Fig. 6a, below. Hatched regions in (b) experience little precipitation (daily precipitation mean is less than 0.275 mm; Fig. 2a, below) or have weak diurnal variations (normalized amplitude is less than 30%; Fig. 4a, below), and hence their times of maximum precipitation amount are considered to be unreliable. (c)–(g) Diurnal cycle functions from IMERG, ERA5, NCAR, CNRM, MRMS, and DPR for each of the numbered regions in (a) and (b); a solid line represents an original cycle, and a dashed line depicts a diurnal cycle fit with a harmonic (24 and 12 h) function. Upward-pointing symbols represent the maximum, and vice versa. Product periods are provided in Table 1. Regions 1–5 are referred to as the Rockies, west Great Plains, east Great Plains, Midwest, and Gulf Stream, respectively, in the text.
Citation: Journal of Climate 34, 12; 10.1175/JCLI-D-20-0966.1
Figure 1 depicts five different regions where the diurnal cycle from IMERG, NCAR-CESM2 AMIP, CNRM-CM6.1 AMIP, ERA5, and DPR is assessed against MRMS; regions with spatial homogeneity in vertical wind velocities (from ERA5) and diurnal phase (from IMERG) are selected. While the Great Plains and Midwest (regions 2–4) show no predominance of updrafts or downdrafts on average, MCSs that form over the Rockies travel eastward over these regions. The nocturnal eastward propagation in diurnal phase depicted by IMERG due to these MCSs is consistent with previous observational studies (e.g., Wallace 1975; Dai et al. 1999; Trenberth et al. 2003; Dai et al. 2007; Dirmeyer et al. 2012; Sungmin and Kirstetter 2018; Tan et al. 2019a; Scaff et al. 2020). Bar charts comparing diurnal parameters between products for each region are provided in Fig. S2 in the online supplemental material. Note that the diurnal cycles of precipitation for NCAR-CESM2 AMIP and CNRM-CM6.1 AMIP are broadly consistent with their respective model’s Historical simulations (i.e., diurnal parameter quantities can vary), while the diurnal cycles for CNRM-CM6.1 AMIP and CNRM-ESM2.1 AMIP closely match.
Regional comparisons of the diurnal cycle highlight that NCAR-CESM2 AMIP, CNRM-CM6.1 AMIP, and ERA5 are more consistent with observations over convection-susceptible regions. However, NCAR-CESM2 AMIP and CNRM-CM6.1 AMIP still exhibit large discrepancies in these regions; over the Rockies, the late afternoon maximum observed by MRMS, IMERG, and DPR (1600 LST) is simulated 4 h later by NCAR-CESM2 AMIP (2000 LST) and 3 h earlier by CNRM-CM6.1 AMIP (1300 LST). Over the Gulf Stream, which lacks MRMS coverage, NCAR simulates distinctively lower precipitation mean and normalized amplitude (NCAR-CESM2 AMIP: 3.7 mm day−1 and 14%; IMERG: 5.2 mm day−1 and 36%, respectively) than the other products. The selected CMIP6 atmosphere-only products tend to compare worst to MRMS over each CONUS region, as highlighted by simulating the smallest means (except over the Rockies) and the smallest normalized amplitudes (except over the Midwest).
IMERG tends to better compare to the CONUS reference, MRMS, than ERA5, NCAR-CESM2 AMIP, and CNRM-CM6.1 AMIP. In particular, IMERG mostly captures the eastward propagation in the time of maximum (MRMS: 1600, 1900, 0300, and 0400 LST for regions 1–4); the exception is that IMERG observes a maximum in precipitation 3 h earlier than MRMS over the east Great Plains, which Sungmin and Kirstetter (2018) suggested may be caused by bias in IMERG’s PMW observations toward the leading convective component of MCSs in this region. In comparison, ERA5 produces an eastward phase jump that is faster than observed, and NCAR-CESM2 AMIP and CNRM-CM6.1 AMIP simulate a false westward phase jump (ERA5: 1500, 1500, 0000, and 0000 LST; NCAR-CESM2 AMIP: 2000, 2000, 1400, and 1400 LST; CNRM-CM6.1 AMIP: 1300, 1300, 1100, and 1100 LST). Like MRMS, normalized amplitude also reduces eastward for IMERG (MRMS: 103%, 89%, 61%, and 26% for regions 1–4; IMERG: 90%, 102%, 71%, and 36%), except for the initial transition from the Rockies; alternatively, ERA5 captures MRMS’s trend (ERA5: 124%, 57%, 48%, and 27%), although it typically differs more from MRMS than IMERG (except over the Midwest). While mainly comparing well to MRMS, IMERG can perform worse than ERA5, NCAR-CESM2 AMIP, and CNRM-CM6.1 AMIP in a few instances. IMERG, ERA5, and CNRM-CM6.1 AMIP all observe/simulate increases in the precipitation mean eastward like MRMS (MRMS: 1.1, 3.1, 4.0, and 4.2 mm day−1; IMERG: 0.9, 2.2, 3.3, and 3.9 mm day−1 for regions 1–4), while IMERG performs worst over the Rockies (MRMS and NCAR-CESM2 AMIP: 1.13 mm day−1, DPR: 0.99 mm day−1, CNRM-CM6.1 AMIP: 0.95 mm day−1, ERA5: 0.94 mm day−1, and IMERG: 0.85 mm day−1). This underestimation of Rockies precipitation reaffirms IMERG’s tendency to underestimate precipitation in mountainous regions (Tapiador et al. 2020), and evaluation of ERA5, NCAR-CESM2 AMIP, and CNRM-CM6.1 AMIP, by precipitation mean in such regions should be treated with caution (Fig. 2). Another instance of IMERG biases affecting model comparisons is over the Midwest; IMERG overestimates the normalized amplitude, failing to capture it unlike ERA5 and NCAR-CESM2 AMIP (MRMS and NCAR-CESM2 AMIP: 26%; ERA5: 27%; CNRM-CM6.1 AMIP: 34%; IMERG: 36%). Overall, these findings reaffirm the skill of IMERG in representing the CONUS diurnal cycle of precipitation as proven by ground-based observations (albeit with some localized biases; Sungmin and Kirstetter 2018; Tan et al. 2019a), and that the use of IMERG is suitable for evaluating models.
Global maps of the precipitation mean from (a) IMERG, (b) ERA5 minus IMERG, (c) NCAR-CESM2 AMIP minus IMERG, and (d) CNRM-CM6.1 AMIP minus IMERG for their respective JJA multidecade study periods. The percentage difference uses IMERG as the denominator. Hatching covers those regions where the daily precipitation mean is less than 0.275 mm for either of the respective products within a panel.
Citation: Journal of Climate 34, 12; 10.1175/JCLI-D-20-0966.1
At present, the DPR exhibits some skill in representing the diurnal cycle over CONUS when subject to harmonic fitting; the harmonic function fit to each region’s original diurnal cycle is depicted in Fig. S3 in the online supplemental material. The DPR compares best to MRMS for precipitation mean across the Great Plains and Midwest and is only second to NCAR-CESM2 AMIP over the Rockies (with an underestimate of 0.14 mm day−1). The DPR is erratic in representing the normalized amplitude: it compares best to MRMS over the Rockies (MRMS: 103%; DPR: 115%) and the east Great Plains (MRMS: 61%; DPR: 62%), but significantly overestimates in the Midwest (MRMS: 26%; DPR: 74%). Even while capturing the amplitude in the east Great Plains, the DPR’s diurnal function is anomalous with a broad peak that spans ~10 h. DPR performance for the time of maximum is erratic too, though typically better than ERA5, NCAR-CESM2 AMIP and CNRM-CM6.1 AMIP (except for the east Great Plains): DPR aligns with MRMS and IMERG over the Rockies, is one hour earlier over the Midwest, and differs by > 3 h over the Great Plains.
5. Global evaluation of the simulated diurnal cycle of precipitation
Diurnal precipitation parameters from NCAR, CNRM, and ERA5 are evaluated against reference IMERG across the globe. From CMIP6, only map plots for CNRM-CM6.1 AMIP and NCAR-CESM2 AMIP are presented because of the broad consistency in the diurnal cycle of precipitation between different simulations from CNRM (CNRM-CM6.1: AMIP, Historical, HR Historical; CNRM-ESM2.1: AMIP) and from NCAR (NCAR-CESM2: AMIP, Historical), respectively (Figs. 3a and 5a and also Fig. S4 in the online supplemental material); consequently, CNRM-CM6.1 AMIP and NCAR-CESM2 AMIP are respectively referred to as CNRM and NCAR when discussing the global results. IMERG results are presented at 0.25° × 0.25° (ERA5’s spatial resolution); the only exception is that IMERG is regridded to the respective CMIP6 product’s spatial resolution for CMIP6 minus IMERG results.
The global distribution of precipitation means from IMERG, NCAR, CNRM, and ERA5 for their respective JJA multidecade study period, represented (a) by boxplots and (b) as a function of the percentile of precipitation mean. For the respective product, only grid pixels with daily precipitation mean exceeding 0.275 mm are included. Whiskers on boxplots extend from the 5th to the 95th percentiles, boxes extend from the 25th to the 75th percentiles, and black circles indicate the 50th percentile for the respective surface (land is red; ocean is blue) and product; these percentiles do not account for varying pixel area by latitude. Percentile functions are deduced as the average precipitation mean from grid pixels with precipitation means within each 5th percentile (0–5th percentile, …, 95th–100th percentile). (c) The difference in percentile functions between NCAR, CNRM, or ERA5 and IMERG, normalized to the IMERG percentile function.
Citation: Journal of Climate 34, 12; 10.1175/JCLI-D-20-0966.1
a. Precipitation mean
Figure 2 depicts the comparison of the precipitation mean across the globe. Hatched regions experience little precipitation (<0.275 mm day−1), and hence their diurnal variations are considered unreliable and their diurnal parameters are excluded from statistics (unless stated). IMERG observes high precipitation amounts across the tropics, especially between 0° and 15°N where the intertropical convergence zone (ITCZ) resides in boreal summer. Dry regions are typically located either side of the ITCZ.
ERA5 better captures observed precipitation than NCAR and CNRM in many regions, especially over land where the models typically simulate less precipitation (with exceptions over Asia). ERA5, NCAR, and CNRM exceed observed precipitation around the Himalaya Mountains, the Andes, and the Rocky Mountains, though this may be due to IMERG underestimating precipitation in mountainous regions (Tapiador et al. 2020). Further exceedance of IMERG precipitation occurs in the drier regions of the tropical and subtropical oceans. Notably, CNRM produces much less precipitation over central Africa (<1 mm day−1) than IMERG, NCAR, and ERA5 (>5 mm day−1). IMERG appears to produce anomalously low JJA precipitation over the South Atlantic and Indian Oceans (45°–60°S), which is not identified at the annual scale (Watters and Battaglia 2020b).
Map plots like Fig. 2 depict regional differences between NCAR/CNRM/ERA5 and IMERG, which can be affected by mismatches in observed and simulated locations/intensities of convection. Figure 3 compares the global distribution of precipitation means from each product using boxplots and percentile function plots (i.e., diurnal parameter average for each 5th percentile of precipitation means, where the parameter is the precipitation mean in this instance), which removes the impact of regional mismatches. The global distribution plots depict the consistency in precipitation means, highlighting that regional discrepancies between NCAR/CNRM/ERA5 and IMERG compensate across global land and ocean. Global mean precipitation for JJA (60°N–S, inclusive of hatched regions and weighted by pixel area) is also consistent between products (~3.2 mm day−1) and falls within the energy budget constraints on annual global mean precipitation (2.7–3.4 mm day−1)/latent heat flux (78–98 W m−2; Stephens et al. 2012). Differences in precipitation means are small across all precipitation regimes (between −25% and +25% of IMERG precipitation for each 5th percentile; Figs. 3b and 3c). Further comparisons of precipitation means are left to future studies, with this study focusing on the diurnal cycle.
b. Diurnal normalized amplitude
Figure 4 depicts the global comparison of diurnal amplitudes (normalized by precipitation means in Fig. 2). IMERG observes that normalized amplitudes are typically larger over land (26%–54%–134%; 5th–50th–95th percentile) than over ocean (14%–28%–66%; Figs. 4a and 5a). These amplitude ranges are similar to the 24-h harmonic mean-to-peak amplitude ranges of 30%–100% over land and 10%–30% over ocean identified by Dai et al. (2007) and Covey et al. (2016) from a gamut of observation products (including TRMM TMPA); this study’s upper extents likely exceed those from the preceding studies since the fitting of harmonics to the diurnal cycle can dampen amplitudes (Tan et al. 2019a). IMERG also identifies a clear difference in oceanic diurnal amplitudes outside of 30°S–45°N, with amplitudes rising from 13%–21%–34% within 60°–30°S to 19%–36%–71% within 30°–0°S; this suggests that oceanic diurnal variations in precipitation are related to insolation.
As in Fig. 2, but for normalized amplitudes; hatching covers regions under the same low-precipitation criterion also.
Citation: Journal of Climate 34, 12; 10.1175/JCLI-D-20-0966.1
As in Figs. 3a and 3b, but for normalized amplitude, using only those grid pixels for which daily precipitation mean exceeds 0.275 mm as previously. Note that (b) presents the average normalized amplitude from grid pixels with precipitation means within each 5th percentile (i.e., average normalized amplitude as a function of precipitation mean).
Citation: Journal of Climate 34, 12; 10.1175/JCLI-D-20-0966.1
ERA5, NCAR, and CNRM typically display smaller diurnal amplitudes over ocean than IMERG (Figs. 4b–d). Damped normalized amplitudes in the NCAR/CNRM AMIP and Historical simulations (Fig. 5a) are likely due to limited diurnal variability in their respective prescribed (monthly mean) and simulated SSTs (to which atmospheric convection is closely coupled; Dai and Trenberth 2004). Over land, NCAR also underestimates normalized amplitudes, while CNRM and ERA5 both typically overestimate across the tropics and central Asia. However, ERA5’s amplitude overestimates are widespread across Northern Hemisphere and tropical land, unlike for CNRM, where insolation is greater in boreal summer; this suggests that ERA5’s convection parameterization is too strong. ERA5 best compares to the median observed amplitude over land (20%–62%–185%) and over ocean (6%–19%–50%), while NCAR performs worst over land (8%–24%–55%) and over ocean (4%–13%–40%; Fig. 5a). These findings are in contrast to the relative agreement in normalized amplitudes between CMIP5 models and TRMM TMPA identified by Covey et al. (2016), although this may be due to their use of harmonics on different models (at higher resolution) and a different observational product. Alternatively, the tendency for ERA5 to overestimate observed amplitudes over land and underestimate over ocean was also identified with the ECMWF operational forecast model (Kidd et al. 2013); underestimation in diurnal amplitudes over the ITCZ is a novel finding of this study.
Figure 5b highlights that normalized amplitudes decrease with increasing precipitation mean over land and ocean (except for NCAR over ocean), before increasing in the wettest regions (>60th percentile, except for NCAR and CNRM over land). NCAR and CNRM fail to fully capture these distinct trends in amplitude, with IMERG and ERA5 suggesting that diurnal normalized amplitudes are greater in the wettest regions on Earth than those with average precipitation. Also, CNRM shows some skill in capturing diurnal amplitudes in the driest land regions (<22nd percentile), while ERA5 exhibits skill in the average precipitation regions over land (40th–60th percentile).
Notably, normalized amplitudes for each product’s multidecade period are smaller than for the product-coincident 2000–08 period by up to a factor of ¼ or ⅛ on average over global ocean or land, respectively (Fig. S1b in the online supplemental material). This may be because the IAV of the time/position of the diurnal maximum may dampen the amplitude over a longer period of averaging. Analyzing multidecade amplitudes is considered to be appropriate since the diurnal cycle signal should be better captured over a longer period.
c. Diurnal time of maximum
Figure 6 depicts the global comparison of the local solar time of maximum. Hatched regions now cover those regions where the normalized amplitude is less than 30% for IMERG or 20% for NCAR, CNRM, and ERA5 (Fig. 4), as well as low-precipitation regions (<0.275 mm day−1; Fig. 2). The regions with amplitudes below the threshold tend to exhibit spatially inhomogeneous phase patterns, which are treated as anomalous due to weak diurnal variations; the thresholds are selected to ensure similar coverage across datasets and tend to cover southern midlatitude ocean regions.
Global maps of the local solar time of maximum from (a) IMERG, (b) ERA5, (c) NCAR-CESM2 AMIP, and (d) CNRM-CM6.1 AMIP for their respective JJA multidecade study period. Hatching covers those regions where the daily precipitation mean is less than 0.275 mm (Fig. 2) or the normalized amplitude is less than a certain threshold (30% for IMERG and 20% for NCAR, CNRM, and ERA5; Fig. 4) for the respective product.
Citation: Journal of Climate 34, 12; 10.1175/JCLI-D-20-0966.1
IMERG observes precipitation over land to maximize from late afternoon to evening (1400–2100 LST), with late-evening to midmorning peaks (2100–0600 LST) close to mountainous regions (i.e., the Rockies, the Andes, and the Himalayas) and regions with varying terrain (central Africa and northeastern South America; Figs. 6a and 7a). Previous observational studies agree with late afternoon to evening peaks over land (e.g., Yang and Slingo 2001; Dai et al. 2007, etc.; see section 1), although IMERG’s northern midlatitude peaks appear to occur a few hours after those from surface weather reports and to better align with convective precipitation peaks alike other satellite products (Dai 2001, 2006; Dai et al. 2007); potential IMERG biases could be due to the heightened sensitivity of PMW and IR measurements to deep convection (Dai et al. 2007), and could be exacerbated by the three-hourly resolution of the weather reports. The nocturnal mountainous peaks are only identified by observations with subdegree spatial resolution (Yang and Slingo 2001; Dai 2006; Covey et al. 2016; Minobe et al. 2020); this highlights the importance of high resolution global observations, as preceding IMERG analyses at 2° and 5° failed to capture these localized nocturnal phase propagations (Watters and Battaglia 2019; Battaglia et al. 2020a). NCAR, CNRM, and ERA5 simulate maximum precipitation over land earlier than IMERG (median pixel difference; NCAR: −1 h; ERA5: −2 h; CNRM: −4 h), reaffirming the tendency for convection-parameterized models to simulate precipitation too early with varying performance (e.g., Trenberth et al. 2003; Dirmeyer et al. 2012; Covey et al. 2016, etc.; see section 1). NCAR simulates diurnal peaks in precipitation from late morning to midevening (1000–2100 LST), with some late-evening to early-morning peaks over central Africa and the Eurasian Plateau (2200–0600 LST; Figs. 6c and 7a). CNRM peaks from midmorning to midafternoon (0800–1600 LST), with evening to early-morning peaks (1900–0200 LST) close to tropical coastlines and the Eurasian Plateau (Figs. 6d and 7a). ERA5 precipitation peaks from late morning to late afternoon (1100–1800 LST) and captures some observed nocturnal regional variations such as the eastward propagation of MCSs from the Rockies and the Andes, though simulates travel faster than observed (0000–0400 LST; Figs. 6b and 7a). ERA5 and CNRM better capture the observed spatial distribution of diurnal phase than NCAR over flatter terrain; ERA5 exhibits some skill at capturing variations in mountainous regions, potentially advantaged by its assimilation of observations, unlike NCAR and CNRM.
The global distribution of the local solar time of maximum from IMERG, NCAR, CNRM, and ERA5 for their respective JJA multidecade period, represented by probability density functions (PDFs) for (a) land and (b) ocean and (c) as a function of the percentiles of precipitation mean. For the respective product, only grid pixels with daily precipitation mean exceeding 0.275 mm and with normalized amplitude > 30% for IMERG or > 20% for NCAR, CNRM, and ERA5 are used (i.e., the grid pixels without hatching in Fig. 6). Percentile functions are deduced as the average time of maximum from grid pixels with precipitation means within each 5th percentile (0th–5th percentile, …, 95th–100th percentile). Figure S4 in the online supplemental material exhibits the PDFs for the remaining NCAR and CNRM simulations from Table 1.
Citation: Journal of Climate 34, 12; 10.1175/JCLI-D-20-0966.1
Over ocean, IMERG observes that precipitation maximizes from early morning to midday (0000–1200 LST), with tropical coastal waters maximizing from midmorning to midday (0600–1200 LST; Figs. 6a and 7b); this is in agreement with other studies (e.g., Yang and Slingo 2001; Dai et al. 2007, etc.; see section 1), though appears to lag surface weather reports by a few hours in open waters (Dai 2001, 2006; Dai et al. 2007). Also, some afternoon/evening phases occur in the Southern Hemisphere. NCAR, CNRM, and ERA5 better compare to the observed time of maximum over ocean than over land (median pixel differences; NCAR: 0 h; ERA5 and CNRM: −1 h); however, they fail to capture the observed bimodal oceanic distribution (peaks at 0100 and 0600 LST). NCAR, CNRM, and ERA5 also estimate oceanic precipitation to maximize from early to late morning (0000–1100 LST), with CNRM better capturing observed coastal late morning maxima (Figs. 6b–d and 7b). Regional differences to IMERG are greater away from continents, with simulated areal coverage of late morning coastal phases smaller than observed (e.g., Gulf of Mexico and the “Maritime Continent”). Simulated spatial distributions are also more homogeneous compared to observations.
IMERG observes similar late afternoon and evening phases across all precipitation regimes over land, while precipitation maximizes later in the morning over wetter regions (Fig. 7c). NCAR, CNRM, and ERA5 do not capture the variation in the time of maximum with increasing precipitation over land or ocean. However, NCAR simulates the observed diurnal phase over the wettest land regions (>85th percentile); NCAR and ERA5 capture the time of maximum over the driest ocean regions (<20th percentile), with CNRM agreeing with IMERG over the wettest ocean regions (>90th percentile).
Future studies could further investigate IMERG’s oceanic bimodal distribution in the time of maximum precipitation (Figs. 6a and 7b), which peaks between 0000 and 0300 LST (maximum at 0100 LST) and between 0400 and 0700 LST (maximum at 0600 LST) and appears to originate from different single-peak cycles in different regions: in the northern midlatitude oceans, 0000–0300 LST maxima typically occur in eastern waters, while 0400–0700 LST maxima occur in western and central waters.
d. Interannual variability of the diurnal cycle
IAV, a measure of the variability in the climate system, quantifies the deviation in the diurnal cycle throughout the respective product’s multidecade period. Precipitation mean and diurnal phase are mostly consistent whether deduced from one multidecade-sampled diurnal cycle (multidecade parameter, as used in preceding results), or from the average parameter across N different yearly sampled diurnal cycles (yearly average parameter, as used in the IAV calculation); this implies that the IAV in the respective parameter is representative of the deviation in the multidecade parameter. However, this is not the case for normalized amplitude, where the yearly averaged amplitude is several times greater than the multidecade amplitude (not shown). Because of the differing multidecade periods between IMERG–ERA5 and NCAR–CNRM in which different El Niño events can have differing effects on the IAV of precipitation, only ERA5 results are directly compared with IMERG in this section (although some NCAR and CNRM results are also shown).
Figure 8 depicts the global distribution of the IAV for each diurnal precipitation parameter; only those pixels that satisfy the multidecade criteria for each parameter are included. IAV distributions for precipitation means and normalized amplitudes are generally small on average (medians < 42% and 36%, respectively, inclusive of NCAR and CNRM results), and relatively consistent between products and between land and ocean; while comparable to IMERG over land, ERA5’s oceanic IAV is smaller. On the other hand, IAVs for the time of maximum are generally large, and more inconsistent between products and between land and ocean. IMERG observes IAVs in the time of maximum of 1.4–4.2–6.4 h (5th–50th–95th percentiles) over land and 3.5–5.5–6.7 h over ocean; ERA5 exhibits smaller IAVs relative to IMERG.
The global distribution of IAV from IMERG, NCAR, CNRM, and ERA5 for their respective JJA multidecade periods, represented by boxplots for (a) precipitation mean, (b) normalized amplitude, and (c) local solar time of maximum. For the respective product, only grid pixels with daily precipitation mean exceeding 0.275 mm (and with normalized amplitude > 30% for IMERG or > 20% for NCAR, CNRM, and ERA5, when considering the IAV in the time of maximum) determined from the multidecade sample are used. Because of the differing multidecade JJA periods between IMERG–ERA5 (2000–19) and NCAR–CNRM (1979–2008), only ERA5’s IAV results can be directly compared with those from IMERG.
Citation: Journal of Climate 34, 12; 10.1175/JCLI-D-20-0966.1
The IAV in the diurnal phase has distinct regional features (Fig. 9). IMERG observes that the diurnal time of maximum accumulation is only consistent from year to year over Central America, the southeastern United States, the Rocky Mountains, southeastern Asia, and eastern central Africa (IAV < 2 h). These regions also experience the greatest diurnal normalized amplitudes (>105%); the density scatterplot highlights that as normalized amplitude increases, the IAV in the diurnal phase decreases. These findings echo those of Dai et al. (1999) for diurnal precipitation occurrence over CONUS. In contrast, ERA5 simulates relatively consistent diurnal phases from year to year across most tropical and Northern Hemisphere land, and tropical oceans west of the continents; furthermore, ERA5 simulates these low IAV regions typically where the normalized amplitude exceeds 56% (IAV < 2 h; Fig. 9d). For both products, the IAV in the diurnal phase is correlated with the number of prominent peaks in the multidecade diurnal cycle (not shown). This suggests that ERA5’s diurnal cycle representation is too simplified, simulating the diurnal phase to be more consistent from year to year than observed across many land regions and the adjacent oceans.
Global map plots of the IAV in the local solar time of maximum from (a) IMERG and (c) ERA5 for JJA 2000–19. Also shown are density scatterplots for the normalized amplitude (determined from the whole 20-yr sample; Fig. 4) vs the IAV in the time of maximum from (b) IMERG and (d) ERA5. For the respective product, only grid pixels with daily precipitation mean exceeding 0.275 mm and with normalized amplitude > 30% for IMERG or > 20% for ERA5 determined from the multidecade sample are used; hatched regions do not satisfy these criteria. The red line in the density scatterplots represents the IAV bin with the highest count for each normalized amplitude bin.
Citation: Journal of Climate 34, 12; 10.1175/JCLI-D-20-0966.1
These results highlight the importance of satellite constellations in consistently tracking global precipitation, which exhibits strong climatological fluctuations in the time of maximum across the globe. Furthermore, this showcases the need for GPM PMW constellation members to be replaced when reaching the end of their lifespan; the GPM constellation is expected to dwindle from 12 different satellites in 2020 to 7 members by 2030 (Watters and Battaglia 2020b), reducing the revisit time of the constellation and its ability to track precipitation on short time scales. Future studies could investigate impacts on the IAV in IMERG’s diurnal cycle caused by the evolution of GPM constellation sensors with time, IMERG’s merging and interpolation of a multitude of satellite retrievals, and noise from a diurnal cycle averaged each year over the 92 days of JJA.
6. Conclusions
This study has evaluated the performance of CMIP6’s NCAR and CNRM models and the ERA5 reanalysis against IMERG observations in representing the diurnal cycle of precipitation accumulation for boreal summer across the globe. To the knowledge of the authors, the study provides the first multidecade global diurnal cycle analysis with IMERG; the first multidecade global evaluation of the diurnal cycle of CMIP6’s NCAR and CNRM models; the first global diurnal cycle evaluation of ERA5; and the first global investigation of the interannual variability of the precipitation diurnal cycle. Only CMIP6’s NCAR and CNRM simulations and ERA5 reanalysis at hourly resolution were used, with IMERG matched to the spatiotemporal resolution of each product for comparison. Differing multidecade periods between IMERG–ERA5 and NCAR–CNRM were selected (Table 1), because of the relative consistency of the diurnal cycle between each respective multidecade period and the coincident 9-yr period between the global-gridded products (Fig. S1 in the online supplemental material). Regions with low precipitation means (<0.275 mm day−1) were excluded from all analyses, as were regions with weak normalized amplitudes (<30% for IMERG and <20% for NCAR, CNRM, and ERA5) when analyzing the time of maximum, to avoid biasing the comparison results.
An initial analysis over CONUS and the Gulf Stream highlighted the tendency for NCAR and CNRM atmosphere-only simulations (NCAR-CESM2 AMIP and CNRM-CM6.1 AMIP) and ERA5 to be more consistent with observations in regions susceptible to convection, though NCAR-CESM2 AMIP and CNRM-CM6.1 AMIP still produced large discrepancies to observations (Fig. 1). The CONUS analysis also demonstrated IMERG’s skill in representing the diurnal cycle of precipitation in this region, including the eastward propagation in the time of maximum precipitation from the Rockies, and its suitability for use in detailed model evaluation due to its general agreement with gauge-adjusted ground-based radar observations from MRMS. However, IMERG can exhibit some localized biases that can affect model evaluation, such as its underestimation of precipitation over the Rockies (which is larger than NCAR-CESM2 AMIP, CNRM-CM6.1 AMIP, and ERA5 underestimates) and across central CONUS, and its 3-h advance of the peak in east Great Plains precipitation, which may be due to a bias in PMW observations toward the leading convective component of MCSs (Sungmin and Kirstetter 2018).
The analysis also provided the first evaluation of the GPM Core Observatory’s DPR in capturing the diurnal cycle of precipitation over CONUS. When fit by a harmonic function with only seven boreal summers of sampling, the DPR tends to outperform IMERG, NCAR-CESM2 AMIP, CNRM-CM6.1 AMIP, and ERA5 in representing the precipitation mean over the Rockies and the central United States, though is erratic in representing the normalized amplitude and time of maximum by region. However, the DPR typically better represents the time of maximum than multiple decades of simulations from NCAR-CESM2 AMIP, CNRM-CM6.1 AMIP, and ERA5. With more years of sampling, it may be possible to use the DPR as a spaceborne reference for the diurnal cycle.
The subsequent global analysis findings include the following:
IMERG, ERA5, NCAR, and CNRM simulations agree on the global mean precipitation for boreal summer (60°N–S; ~3.2 mm day−1), and the global distribution of precipitation, though disagree significantly at the regional scale (Figs. 2 and 3). Key regional discrepancies include ERA5, NCAR, and CNRM exceeding observed precipitation over drier regions of subtropical/tropical oceans, and the Himalayas, the Andes, and the Rockies; model exceedance in mountainous regions may be due to low IMERG biases, however. Low precipitation biases from IMERG in the South Atlantic and Indian Oceans (45°–60°S) are also identified.
The diurnal cycle of precipitation is broadly consistent between coupled, atmosphere-only and high-resolution versions of the CNRM model, and between coupled and atmosphere-only versions of the NCAR model, though differs between these models (Figs. 3a and 5a, and also Fig. S4 in the online supplemental material). The following NCAR and CNRM global results are derived from atmosphere-only simulations (NCAR-CESM2 AMIP and CNRM-CM6.1 AMIP, respectively), although variations (if any) with coupled or high-resolution simulations are typically small.
IMERG identifies diurnal precipitation amplitudes (normalized by the mean) to be greater over land (26%–134%; 5th–95th percentile) than over ocean (14%–66%), with a significant reduction south of 30°S over ocean (Figs. 4 and 5). Furthermore, IMERG observes normalized diurnal variations in precipitation to be greater in the wettest regions on Earth than in regions that receive average precipitation. Also, IMERG observes precipitation to peak over land at 1400–2100 LST, and 2100–0600 LST close to mountainous regions (Rockies, Andes, Himalayas) and regions with varying terrain (central Africa, northeastern South America; Figs. 6 and 7). Over ocean, IMERG observes precipitation to peak at 0000–1200 LST, with peaks closer to midday in coastal regions. No distinctive variation in the time of maximum as a function of mean precipitation amount is identified over land, while wetter ocean regions experience maximum precipitation later in the morning.
In terms of diurnal normalized amplitudes over land, ERA5 overestimates across the tropics and Northern Hemisphere, CNRM overestimates over the tropics and central Asia, and NCAR underestimates everywhere (Figs. 4 and 5). Over ocean, ERA5, NCAR, and CNRM underestimate normalized amplitudes everywhere. ERA5’s global distribution of normalized amplitudes (20%–185% over land; 6%–50% over ocean) compares better to IMERG than the selected CMIP6 simulations (by comparison of land/ocean medians).
NCAR, ERA5, and CNRM simulate precipitation over land earlier than observed by IMERG, with average differences in the time of maximum of −1, −2, and −4 h, respectively (Figs. 6 and 7). Precipitation peaks between 1000 and 2100 LST for NCAR (2200–0600 LST over central Africa and the Eurasian Plateau), 0800 and 1600 LST for CNRM (1900–0200 LST over tropical coastlines and the Eurasian Plateau), and 1100 and 1800 LST for ERA5 (0000–0400 LST over the Rockies and the Andes). NCAR produces the poorest spatial distribution of diurnal phases over flatter land, whereas ERA5 exhibits some skill in capturing mountainous nocturnal propagation unlike NCAR and CNRM.
ERA5, NCAR, and CNRM better capture the time of maximum precipitation over ocean than over land; NCAR matches the IMERG phase on average, while ERA5 and CNRM have an average phase difference to IMERG of −1 h (Figs. 6 and 7). All simulate oceanic precipitation to peak between 0000 and 1100 LST, similar to IMERG, although they fail to capture the observed bimodal distribution of phases with peaks at 0100 and 0600 LST.
Interannual variability (IAV) in the precipitation mean and normalized amplitude is small on average for IMERG, NCAR, CNRM, and ERA5 (<42% of the multidecade parameter; Fig. 8). However, IMERG observes the IAV in the time of maximum to be highly variable. IMERG suggests that the diurnal phase is only consistent from year to year (IAV < 2 h) over Central America, southeastern United States, the Rockies, southeastern Asia, and eastern central Africa, where the diurnal amplitude (from the multidecade sample) is similar in magnitude to the diurnal precipitation mean (>105% of the mean; Fig. 9). ERA5’s representation of the diurnal cycle is too simplified, simulating year-to-year consistency in diurnal phases across land and ocean regions more than observed (i.e., where the amplitude typically exceeds 56% of the precipitation mean).
IMERG validation is of paramount importance for model evaluation studies. The IMERG–MRMS comparison, and other preceding validation studies (e.g., Tan et al. 2016; Dezfuli et al. 2017; Sungmin and Kirstetter 2018; Tan et al. 2019b; Tang et al. 2020), demonstrate IMERG’s capability to represent precipitation, although they also identify its pitfalls. Further validation studies are required to assess IMERG’s skill in capturing the diurnal cycle across regions other than CONUS, Africa, and China, and to identify biases that could be misinterpreted as model inaccuracies.
There are many challenges to determining the diurnal cycle from a single low-Earth-orbit satellite (including spatially inconsistent sampling that can introduce noise into the cycle at fine scales; Negri et al. 2002); the results have shown that even 7 years of DPR observations are insufficient to properly sample the diurnal cycle. A constellation of satellites can improve the spatial coverage and revisit time of precipitation observations (Hou et al. 2014); the augmented satellite constellation coverage from IMERG has strong skill in capturing the diurnal cycle over CONUS, and multiple decades of consistent coverage has enabled discovery of the large yearly fluctuations in the time of precipitation maximum. Satellite constellation challenges include potentially observing maximum precipitation later than at the surface since their PMW and IR sensors respectively sense cloud tops and hydrometeors aloft (Dai et al. 2007), and a lack of subdaily calibration in their precipitation products; however, phase lags may be reduced with enhanced PMW contribution in such products (Tan et al. 2019a). Continuous operations and renewal and deployment of GPM-like constellations, including multiwavelength Doppler radars (Battaglia et al. 2020b), are of paramount importance for diurnal cycle studies and the evaluation of models. This should be considered in the current studies in preparation of the NASA Aerosol, Cloud, Convection and Precipitation (ACCP) mission.
The results of this study have many potential impacts. Highlighted deficiencies in the state-of-the-art models and reanalysis need to be tackled to improve their realism, especially in light of the extensive use of CMIP6 models for simulating future climate change scenarios (Eyring et al. 2016). Future studies could consider further ground-based validation of the diurnal cycle of precipitation from IMERG, CMIP6, and ERA5 over different locations. Other studies could further investigate the interannual variability in the diurnal cycle and the impact of IMERG’s passive microwave morphing scheme on this variability.
Acknowledgments
Daniel Watters was funded by a Natural Environment Research Council studentship awarded through the Central England NERC Training Alliance (CENTA; Grant NE/L002493/1) and by the University of Leicester. Alessandro Battaglia’s work was supported by the European Space Agency under the activity “RainCast” (Contract 4000125959/18/NL/NA). Richard P. Allan was funded by the National Centre for Earth Observation Grant NE/RO16518/1. The authors thank three anonymous reviewers for their helpful comments and recommendations, which greatly helped to improve the paper. The authors thank Kamil Mroz for suggesting the inclusion of MRMS in the CONUS analysis and for help with accessing the MRMS files. The version-6B level-3 IMERG data and the version-6A level-2 DPR data were provided by the NASA/Goddard Space Flight Center and PPS, which develop and compute the data products as a contribution to GPM, and are archived at the NASA GES DISC. The authors acknowledge the World Climate Research Programme, which, through its Working Group on Coupled Modelling, coordinated and promoted CMIP6. The authors thank the climate modeling groups for producing and making available their model output, the Earth System Grid Federation (ESGF) for archiving the data and providing access, and the multiple funding agencies who support CMIP6 and ESGF. This publication contains Copernicus Climate Change Service information (2020); neither the European Commission nor ECMWF is responsible for any use that may be made of the Copernicus information or data it contains. This research used the SPECTRE High Performance Computing Facility at the University of Leicester.
Data availability statement
All data products are freely available from their respective data sources listed in Table 1. The NCAR data are available under the CC BY-SA 4.0 license (https://creativecommons.org/licenses/by-sa/4.0/), and the CNRM-CERFACS data are available under the CC BY-NC-SA 4.0 license (https://creativecommons.org/licenses/by-nc-sa/4.0/).
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